Proposed Title 1: - Queen's University

FLUID EVOLUTION AND STRUCTURAL CONTROL ON URANIUM
DEPOSITS IN SUCCESSOR BASINS IN NORTHERN CANADA AND
NORTHERN AUSTRALIA
by
Serigne Dieng
A thesis submitted to the Department of Geological Sciences and Geological
Engineering in conformity with the requirements for
the degree of Doctor of Philosophy
QUEEN’S UNIVERSITY
Kingston, Ontario, Canada
(August, 2012)
Copyright © Serigne Dieng, 2012
i

Bolger open pit, Beaverlodge area, Northern Saskatchewan, Canada.
ii

Abstract
Uranium deposits associated with Paleoproterozoic successor basins were
investigated using structural, petrographic, geochronological and geochemical relationships
to understand the character and timing of ore-forming fluids and the structural control on
uranium mineralization. The work focused on two successor basins that share similar
geological characteristics: the Martin Lake Basin in the Beaverlodge area in Canada, and
the El Sherana Basin in the South Alligator River area in Australia.
The Beaverlodge area records six temporally distinct stages of U mineralization
spatially associated with the Martin Lake successor basin. Early minor stages are hosted in
cataclasite and veins at ca. 2.29 Ga and in albitized granite in the Gunnar deposit between
ca. 2.3 Ga and 1.9 Ga, which predates the main stage of U mineralization of hydrothermal
breccias that formed at ca. 1.85 Ga. Later stages of mineralization are related to minor veins
at ca. 1.82 Ga linked to alkaline mafic dikes associated with the Martin Lake Basin and to
minor veins at ca. 1.62 Ga corresponding to the timing of unconformity-type U
mineralization in the overlying Athabasca Basin. The main breccia-type U mineralizing
event that affected all deposits in the Beaverlodge area formed at ca. 1.85 Ma from
metamorphic fluids at ca. 330 o C linked to metasomatism during regional metamorphism of
the Trans-Hudson Orogen. The ore-forming fluids were likely derived from metamorphic
remobilization of pre-existing U-rich basement rocks, and ascended upward along deep
fracture systems that resulted from brittle reactivation of early ductile shear zones.
The main event of U mineralization in the South Alligator River area formed at ca.
1.82 Ma, subsequent to deposition of the El Sherana Group at 1.84-1.83 Ma. The formation
iii

of these deposits is related to fluids derived from diagenetic processes in sandstone of the
El Sherana Group. Mineralization formed when a 250 o C, low latitude, oxidizing, U-bearing
basinal brine from diagenetic aquifers in the Coronation sandstone descended downward
into the unconformity along fracture systems created by brittle reactivation of the El
Sherana-Palette fault system.
Uranium deposits associated with successor basins in the Beaverlodge and South
Alligator River area are older than those in the U-rich Athabasca and Kombolgie basins.
Rocks that host these deposits have been folded, and then exhumed during subsequent
tectonic events. These older U deposits can be considered as a potential source for detrital
uraninite that fed sediments of the Athabasca and Kombolgie basins and therefore
contributed to the inventory of uranium that formed unconformity-related U mineralization
in the younger basins. Therefore, the occurrence of older U mineralization associated with
successor basins can be considered as positive criterion for exploration of unconformityrelated
U mineralization in younger Paleoproterozoic basins.
iv

Co-Authorship
This thesis and the manuscripts contained herein are the work of Serigne Dieng.
All chapters are co-authored by Kurt Kyser and Laurent Godin (thesis supervisors) who
provided scientific guidance, discussion, and editorial assistance.
v

Acknowledgements
I would like to express my sincere and profound gratitude to my thesis supervisors
Kurt Kyser and Laurent Godin for giving me this unexpected opportunity to be part of this
excellent Ph.D. research project and to attend this world’s leading university. Your
guidance, assistance, patience, and constant support will be always acknowledged. Merci.
This project was made possible through the generous financial support by the Natural
Sciences and Engineering Research Council of Canada (NSERC) and Cameco Corporation.
The Geological Sciences Department at the University of Saskatchewan and the
Northern Territory Geological Survey in Australia generously provided samples necessary
for this research.
Red Rock Energy and Paul Stewart are thanked for their generous field support.
Special thanks to my Queen’s Facility for Isotope Research lab family, specifically
April Vuletich, Don Chipley, Kerry Klassen, Allison Laidlow, Bill McFarlane, Kristin
Feige, Evelyne Leduc, and Sandeep Banerjee who provided great assistance and guidance
for isotopic analytical methods. Peter Jones at Carleton University, and Alan Grant and
Brian Joy at Queen’s provided valuable assistance with electron microprobe and XRD
analyses.
Particular thanks are due to Steve Beyer, Dan Jiricka, Laurent Scanlan, and Don
Chipley for their constructive editorial comments that greatly improved this thesis.
I would like to extend my gratitude to the enthusiastic U research group specially, Ronald
Ng, Yulia Uvarova, Steve Beyer, Paul Alexandre, Valeria and Alexy Li, Paul Stewart,
vi

Sarah Rice and Jonathan Cloutier, and the tectonic research team, Carl Nagy and Borja
Antolin Tomas. You are so willing to support one another and happy to share your
acknowledge and experience and I have taken fully advantage of it.
I gratefully acknowledge the administrative staffs, Kelly Smith, Linda Brown, Joan
Charbonneau and Dianne Hyde. Thanks for your love, your support and your constant
encouragement during the time I spent at Queen’s University.
To my thesis committee members, Mostafa Fayek, John Peacey, Ron Peterson, and
Herb Helmstaedt, thanks so much for the time you spent evaluating and improving this
work.
I would like to express my profound gratitude to Dennis Jones, former Vice-President
Exploration of Iamgold and IAMGOLD Corporation for first giving me the great
opportunity to complete the M.Sc. Mineral exploration program at Queen’s University.
To my family, my wonderful wife Die Aissatou and my lovely children Seydina,
Diarra, Cheikh and Rassoul, I hope you have spent great time in Canada, loving the winter
and supporting dad through his research. Thanks so much for your patience while dad spent
so much time at office. I love you so much and am very proud of you.
I would like to honor through this thesis the memory of my Mom and my Dad.
Thanks for your love and affection. You taught me to do the right things; I will always be
grateful.
vii

Statement of Originality
I hereby certify that all of the work described within this thesis is the original work of the
author. This research does not support previous degree requirements. Any published (or
unpublished) ideas and/or techniques from the work of others are fully acknowledged in
accordance with the standard referencing practices.
(Serigne Dieng)
(August, 2012)
viii

TABLE OF CONTENTS
Abstract………………………………………………………..……………………………iii
Co-Authorship……………………………………………………………………………….v
Acknowledgements………………………………..………………………….…………….vi
Statement of Originality……………………………………..………..………...…………viii
Table of Contents……………………………………………………..…………………….ix
List of Figures……………………………………………………...…………………...….xv
List of Tables………………………………………………………...…………..………xviii
CHAPTER 1……………………………………………………………………..…………1
INTRODUCTION……………………………………………………………………….....1
1.1 Geological setting of the Beaverlodge area………………………..……..……...……2
1.1.1. Regional geological and structural setting……………………..….……….….2
1.1.2. Uranium mineralization…………………………………...…………….…….5
1.2 Geological setting of the South Alligator Mineral Field area………………………...7
1.2.1 Regional geological and structural setting………………………...………..…7
1.2.2. Uranium mineralization……………………………...…………………..……9
1.3 Uranium mineralized systems in the Athabasca and Kombolgie basins………………11
1.4 Uranium mineralized systems in the successor basins…………………...……………14
1.5 Purpose of this Thesis…………………...…………………………………………….15
1.6 Thesis Structure………………………………………………..………………………17
CHAPTER 2………………………………………………..……………………………..19
TECTONIC HISTORY OF THE NORTH AMERICAN SHIELD RECORDED IN
URANIUM DEPOSITS IN THE BEAVERLODGE AREA, NORTHERN
SASKATCHEWAN, CANADA
Abstract…………………………...…………………………………………………….….19
2.1. Introduction……………………………………………………………………………20
2.2. Geologic Setting…….…………………………………………………………………21
2.2.1. General geology……………………………………………………….………21
2.2.2. Previous models age for U mineralization in the Beaverlodge area……….…26
2.3. Methodology…….……………………………………………………………….……28
ix

2.3.1. U-Pb dating of uranium-rich minerals by LA-HR-ICP-MS…………….…….28
2.3.2. Electron-microprobe procedure and calculations of chemical Pb age……..…29
2.4. Results…………………………...……………………………………………….……30
2.4.1. The Main Ore shear zone.……………………………………………….….…30
2.4.1.1. Geology of the Cinch Lake deposit……………………………..……30
2.4.1.2. Structural and metamorphic relationships in the Main Ore shear
zone…………………………………………………………………..34
2.4.2. The Saint Louis fault.…………………………………………………….……39
2.4.2.1. Geology of the Ace-Fay-Verna deposits……………………….….…39
2.4.2.2. Structural and metamorphic relationships in the Saint Louis fault….39
2.4.3. Paragenesis of the alteration and ore minerals and type of U mineralization....45
2.4.3.1. Stage 1. Mylonitization……………………………………...…….…45
2.4.3.2. Stage 2. Cataclasite deformation…………………………...……...…47
2.4.3.3. Stage 3. Early tensional ±U 2 veins formation…………….....…….…47
2.4.3.4. Stage 4. Granite-related metasomatic alteration………………….….47
2.4.3.5. Stage 5. Brecciation……………………………………...………..…48
2.4.3.6. Stage 6. Mafic volcanism………………………………...………..…48
2.4.3.7. Stage 7. Late U 6 uraninite veins………………………...……..…..…49
2.4.4. Geochronology of uraninite and isotopic systematics…………...….…………51
2.4.4.1. Geochronology of U-rich minerals by LA-HR-ICPMS...……..……..51
2.4.4.1.1. Geochronology of the cataclasite-type ±U 1 ………………….…55
2.4.4.1.2. Geochronology of the early tensional vein-type ±U 2 ……….…..56
2.4.4.1.3. Geochronology of the granite-related metasomatic-type U 3 ……56
2.4.4.1.4. Geochronology of the breccia-type U 4 …………...……..………56
2.4.4.1.5. Geochronology of the volcanic-type ±U 5 ………...………….…56
2.4.4.1.6. Geochronology of the Athabasca-related ±U 6 …...…………...…57
2.4.4.1.7. Post-mineralization alteration events............................................57
2.4.4.2. Chemical Pb age of the uranium mineralization…...…….………..…60
2.5. Discussion……………………………………………………………………………..65
2.5.1. Interpretation of the Main Ore shear zone and Saint Louis fault……………..65
x

2.5.2. Temporal relationships of fault activities and U mineralization to regional
tectonic events…………………………...…………...………..………………69
2.6. Conclusions……………………………………………………………………..…..…78
CHAPTER 3…………………………….……………………………………………..…80
GENESIS OF MULTIFARIOUS URANIUM MINERALIZATION IN THE
BEAVERLODGE AREA, NORTHERN SASKATCHEWAN, CANADA
Abstract………………………………………………………………………….……...…80
3.1. Introduction……………………………………….………………………..…..……82
3.2. Geologic Setting………………………………….………….…………..….….……83
3.2.1. General geology………………………….……………….…….……….….…83
3.2.2. Uranium mineralization………………….………………..………………..…86
3.3. Methodology………………….……………………………………………….…..…87
3.4. Results………………….……………………………………………….……….…...90
3.4.1. Paragenesis of the alteration minerals and types of U mineralization……...…90
3.4.2. Crystal Chemistry………………………….……………….……………….…96
3.4.2.1. Mineral chemistry of uraninite and brannerite…….……………...…96
3.4.2.2. Chlorite Crystal Chemistry……….……………….……………..…100
3.4.3. Isotopic compositions of minerals and fluids involved in the U
mineralization…….………..…………………………………………….…...105
3.4.3.1. Oxygen and carbon isotopes of calcite……………………….….…105
3.4.3.2. Oxygen and hydrogen isotopic compositions of chlorite….……….109
3.4.4. Rare earth elements geochemical characteristics of the U mineralization…..112
3.5. Discussion………………….……………………….……………………………....117
3.5.1. Early U mineralization…………………….……………….………...………118
3.5.2. Formation of breccia-type U deposits, the major U mineralization…………124
3.5.3. Later basin-related U mineralization…….……………….……………...…..127
3.5.4. Late alteration events…….……………….……………………………….....129
3.6. Conclusions…….……………….…………………………………………………..130
xi

CHAPTER 4……………………………………………………………………….…….132
FLUID EVOLUTION AND GENESIS OF URANIUM MINERALIZATION IN THE
SOUTH ALLIGATOR VALLEY AREA, NORTHERN TERRITORIES,
AUSTRALIA
Abstract……………………………………………………………………………..….…132
4.1. Introduction………………………………………………………………………..…133
4.2. Geologic Setting…………………………………………………………………...…136
4.2.1. General geology…………………………………………………………..…136
4.2.2. Uranium mineralization………………………………………………………138
4.3. Characteristics of selected uranium deposits…………………………………..….…140
4.3.1. Coronation Hill uranium deposit……………………………………….….…140
4.3.2. El-Sherana uranium deposit……………………………………………….…142
4.4. Methodology…………………………………………………………………………144
4.5. Results……………………………………………………………………………..…146
4.5.1. Mineral Paragenesis…………………………………………………….……146
4.5.1.1. Coronation Hill uranium deposit……………………………………146
4.5.1.1.1. Pre-ore alteration……………………………………………….146
4.5.1.1.2. Uranium and gold mineralization……………………………...150
4.5.1.1.3. Post-ore alteration…………………………………..……….…152
4.5.1.2. El-Sherana uranium deposit……………………………………..….153
4.5.1.2.1. Pre-ore basement hydrothermal alteration…………………..…155
4.5.1.2.2. Pre-ore diagenetic alteration of the Coronation sandstone….…155
4.5.1.2.3. Uranium mineralization……………………………………..…157
4.5.1.2.4. Post-Ore alteration………………………………………..……159
4.5.2. Crystal chemistry of the alteration minerals…………………………………159
4.5.2.1. Coronation Hill uranium deposit……………………………………159
4.5.2.1.1. Uraninite Crystal Chemistry…………………………...………159
4.5.2.1.2. Chlorite crystal chemistry………………………………...……162
4.5.2.2. El-Sherana Uranium deposit…………………………………..……163
xii

4.5.3. Isotopic compositions of minerals and fluids involved in the U
mineralization……………………………………...…………..……………..164
4.5.4. Geochronology of uraninite and isotopic systematics………………..………166
4.5.4.1. U-Pb geochronology of U-rich minerals by LA-HR-ICP-MS…...…167
4.5.4.2. Pb-Pb geochronology of galena and uraninite by LA-HR-ICP-MS..171
4.5.4.3. Chemical Pb age of the uranium mineralization……………………173
4.6. Discussion……………………………………………………………….…..……...174
4.6.1. Basement metamorphism and basin diagenesis……………..……….………175
4.6.2. Hydrothermal alteration and uranium mineralization….……………….……179
4.6.3. Late stage alteration and resetting events……………………………….……182
4.7. Conclusions…………………………………………………………………………185
CHAPTER 5………………………………………………………………......…………188
GENERAL DISCUSSION
5.1. Introduction…………………………………………….………………………...…188
5.2. U mineralizing system in Paleoproterozoic successor basins…………..…………189
5.2.1. Early U mineralization………………………………………………….....…191
5.2.1.1. Granite-related uranium mineralization…………...……………..…192
5.2.1.2. Metamorphic-related uranium mineralization………………………194
5.2.1.2.1. Early-vein and cataclasite-type uranium mineralization….194
5.2.1.2.2. Breccia-type uranium mineralization………….……….…194
5.2.2. Successor basin-related U mineralization……………………………………196
5.2.2.1. Volcanic-related U mineralization……………………………….…196
5.2.2.2. Unconformity-related U mineralization…………………..………...197
5.2.3. Late alteration events……………………………………………………..….198
5.3. Implication for uranium metallogeny in others Paleoproterozoic successor basins: the
case of Finland and Guyana………………..…………………………………….…201
5.3.1. Uranium metallogenic in Paleoproterozoic successor basins in Finland….…201
5.3.2. Uranium metallogeny in Paleoproterozoic basins in Guyana………….…….205
xiii

CHAPTER 6……………………………………………………………………………..209
GENERAL CONCLUSION
References……………………………...…………………………………………………212
Appendix A. Isotopic data and apparent ages for various generations of uraninite in the
Beaverlodge area……………….……………………………………..……………239
Appendix B. REE contents of various generation of uraninite from deposits of the
Beaverlodge area…………………………………………………...………………246
Appendix C. REE characteristic parameters of various generation of uraninite from deposits
of the Beaverlodge area……………………………………………...……………..248
Appendix D. Electron microprobe analyses of various chlorite phases in deposits of the
Beaverlodge area…………………….………………………………..……………250
Appendix E. Electron microprobe data and temperatures of various chlorite phases from
deposits of the Beaverlodge area...............................................................................255
Appendix F. Results of the electron microprobe analyses for different uraninite occurrences
in the Beaverlodge area…….……………………………………………..………..259
Appendix G. Isotopic data and apparent ages for various generations of uraninite from the
South Alligator River area…….………………………...………………………….263
Appendix H. Electron microprobe data and temperatures of various chlorite phases from
deposits of the South Alligator River area…………………………..………….…..267
Appendix I. Structural measurements (strike and dip) and stereoplot of different structures
from the Cinch Lake deposit………………………………………………………..271
xiv

List of Figures
Figure 1.1. Generalized geological map of the Western Churchill province, Canada………3
Figure 1.2. Regional geology of the Pine Creek Inlier……………………………..……….8
Figure 1.3. Genetic model for unconformity-type U deposit………………………………12
Figure 1.4. Schematic representation of the location of various types of U deposits……...13
Figure 1.5. Geological disciplines used in this study to evaluate the character and formation
of uranium deposits in successor basins……………………………………….…….15
Figure 2.1. Simplified geological map of the southwestern Churchill province, Canada…23
Figure 2.2. Simplified geological map of the Beaverlodge area………………...…………25
Figure 2.3. Detailed geologic map of the Cinch Lake area.………………...…………...…31
Figure 2.4. Photographs of the three main lithostructural units at the Cinch Lake area…...33
Figure 2.5. Various structural and textural relationships along the Main Ore shear zone at
the Cinch Lake deposit.………………...………………….…………………………...…..37
Figure 2.6. A. Detailed geologic map of the Ace-Fay-Verna deposits…………………….40
Figure 2.7. Microphotograph of various structural and textural relationships along the Saint
Louis fault at the Ace-Fay-Verna deposit. .…………………………………………....…..43
Figure 2.8. Generalized paragenesis of the uranium mineralization, metamorphic
relationships and deformation sequences in the Beaverlodge area……….…….46
Figure 2.9. Microphotograph of typical mineral assemblages and crosscutting relationships
from the Ace-Fay-Verna, Cinch Lake and Gunnar uranium deposits……….…50
Figure 2.10. Backscattered Electron Microscope (BSEM) of U-rich minerals……………54
Figure 2.11. U-Pb concordia diagrams from in situ isotopic analysis by LA-HR-ICP-MS of
U from various deposits in the Beaverlodge area………………………………59
Figure 2.12. Plot of element contents in uraninite as a function of chemical Pb
ages…………………………………………………………………………...…64
Figure 2.13. Schematic cross-sections illustrating the general tectonic evolution and timing
of the uranium mineralization in the Beaverlodge area…………………………68
Figure 2.14. Regional geological map of the North American shield……………………..71
Figure 2.15. Distribution of 207 Pb/ 206 Pb ages for 260 uraninite grains along with the timing
of various uranium mineralization and tectonic events…………………………77
xv

Figure 3.1. Generalized geological map of the Western Churchill Province, Canada….….83
Figure 3.2. Simplified geological map of the Beaverlodge area……….………………..…85
Figure 3.3. Mineral paragenesis of the Beaverlodge U deposits……….…………….….…91
Figure 3.4. Photomicrographs of typical mineral assemblages ……………………….…...94
Figure 3.5. Content of substituting elements in U as function of the chemical Pb age……97
Figure 3.6. Diagrams showing the compositional variation of chlorite phases.......….…..102
Figure 3.7. Calculated δ 18 O and δ 13 C values of mineralizing fluids in equilibrium with
carbonate minerals……….……………………………………………....…………106
Figure 3.8. Calculated δ 18 O and δ 2 H values of mineralizing fluids in equilibrium with
chlorite minerals……...…………………………………………………………….110
Figure 3.9. Diagrams showing chondrite normalized REE compositions of uraninite…..113
Figure 3.10. Chondrite-normalized REE patterns in uraninite ……….……………….…115
Figure 3.11. Conceptual genetic model for U mineralization in the Beaverlodge area…..121
Figure 4.1. Geological map of the South Alligator River area……………………….…..135
Figure 4.2. Geological plan of the Coronation Hill deposit……………………….……..141
Figure 4.3. Geological cross-section of El Sherana U deposits…………………………..143
Figure 4.4. General mineral paragenesis of the Coronation Hill deposit……..……….…147
Figure 4.5. Photomicrographs of typical mineral alteration phases of the pre-ore stage...149
Figure 4.6. Photomicrographs of typical mineral alteration phases of the syn-ore stage...151
Figure 4.7. Photomicrographs of typical mineral alteration phases of the post-ore stage..153
Figure 4.8. General mineral paragenesis of the El Sherana deposit………………………154
Figure 4.9. Microphotograph of typical mineral assemblages and crosscutting relationships
of the pre-, syn, and post-ore stage in the El Sherana deposit…………………...…156
Figure 4.10. Photomicrographs of mineral assemblages of the Coronation sandstones….158
Figure 4.11. Calculated δ 2 H and δ 18 O values of fluids in equilibrium with clay minerals.165
Figure 4.12. U-Pb concordia diagrams from in situ isotopic analysis by LA-HR-ICP-MS of
U-rich minerals from the Coronation Hill and El Sherana deposits …………..…..170
Figure 4.13. Pb-Pb isochron diagrams of galena and uraninite from Coronation Hill...…172
Figure 4.14. Plot of element contents in uraninite as a function of chemical Pb ages……174
Figure 4.15. Conceptual genetic model for U mineralization in the SAVMF……………178
xvi

Figure 4.16. Distribution of 207 Pb/ 206 Pb ages and timing of various U mineralization and
tectonic events that affected the South Alligator Valley area………………………184
Figure 5.1. Generalized model for uranium mineralizing system in Paleoproterozoic
successor basins.……………………………………………………………...…….189
Figure 5.2. Geologic cross-section through the Gunnar deposit …………………………193
Figure 5.3. Schematic illustration of the tectonic evolution of the Main Ore Shear Zone and
the Saint Louis Fault.……………...…………………….……………..…………...195
Figure 5.4. Bedrock of Finland……………………………………………………….…..202
Figure 5.5. Schematic Karelian stratigraphy, lithology, and U occurrences in the Koli area,
eastern Finland………..………………………………..……...…………..………..203
Figure 5.6. Distribution of the Roraima Supergroup in northern South America………...206
Figure 5.7. Geologic setting of the Aricheng U deposit ……………………....................208
xvii

List of Tables
Table 1.1. Uranium production of the Beaverlodge area………..………………..…………6
Table 1.2. Production for U deposits in the Northern Territory……..…………..…………10
Table 1.3. Amount of U resources and average grades………………………………….…13
Table 1.4. Global U production and resources by deposit type……………………………14
Table 2.1. Analytical data from the U/Pb LA-HR-ICP-MS analysis of various uraninite
occurrences in the Beaverlodge area…………………………..…...………...…….53
Table 2.2. Summary of the U-Pb concordia results of U-rich minerals for various events..55
Table 2.3. Average chemical composition and calculated chemical Pb ages of different U
occurrences in the Beaverlodge area……………………………………..………...63
Table 3.1. Electron microprobe analysis and chemical composition of U and brannerite..100
Table 3.2. Temperatures of formation, and average structural formulas…………………100
Table 3.3. Representative electron microprobe analysis of syn-ore chlorite phases…..….104
Table 3.4. Representative electron microprobe analysis of various chlorites affected by late
low-temperature alteration phases…………………………………....………..….105
Table 3.5. Measured δ 18 O and δ 13 C for calcite and calculated δ 18 O fluid and δ 13 C fluid values
for fluids in equilibrium with carbonate minerals…………………..………….…108
Table 3.6. Measured δ 18 O and δ 2 H for chlorite and calculated δ 18 O and δ 2 H values for
fluids in equilibrium with chlorite minerals…………………………..…………..111
Table 3.7. Characteristic of REE compositions uraninite………………………………...114
Table 3.8. REE contents of uraninite from different generations of U deposits……….…117
Table 3.9. Summary of the paragenetic mineral assemblages and timing of the U
mineralization……….………………………………………...…………..…..…..118
Table 4.1. Results of the electron microprobe analyses for uraninite occurrences in the
Coronation Hill deposit…………………………………………………..……….162
Table 4.2. Representative electron microprobe analyses of various chlorite phases from the
Coronation Hill and El Sherana deposits………………………………….……...163
Table 4.3. Measured δ 18 O and δ 2 H for muscovite and calculated δ 18 O and δ 2 H values for
fluids in equilibrium with minerals……………………………………….………166
xviii

Table 4.4. Isotopic data of the U-Pb LA-HR-ICP-MS analysis and apparent-ages for
uraninite from the Coronation Hill and El Sherana deposits…………………….…168
Table 4.5. Summary of the U-Pb concordia results of U-rich minerals for various events in
the Coronation Hill and El Sherana deposits. ………………………………….…..170
Table 4.6. Isotopic analyses data of the Pb-Pb LA-HR-ICP-MS analysis of galena from the
Coronation Hill deposit………………………………………………………….….173
Table 4.7. Summary of the major results presented in this Chapter..…………….…..…..175
xix

CHAPTER 1
INTRODUCTION
The Athabasca Basin in Canada and the Kombolgie Basin in Australia are late
Paleoproterozoic basins that host world-class unconformity-type uranium deposits that
contribute to up to 35% of the global uranium market (e.g. Dahlkamp, 1993; Ghandi,
2007). These deposits are spatially associated with an older uranium mineralizing system
that occurs in Paleoproterozoic successor basins; the Martin Lake Basin in the Beaverlodge
area, Northern Saskatchewan, Canada, and the El Sherana Basin in the South Alligator
River area, Northern Territories, Australia. These successor basins formed synchronous or
after major orogenic events (examples of such orogens are the Trans-Hudson Orogen in
Canada and the Top-End Orogen in Australia; Needham, 1985; Hoffman, 1989) and
therefore may be associated with local rifting and volcanism (Needham, 1985; Hartlaub et
al., 1999; Moreilli et al., 2001).
Unconformity-type uranium deposits associated with the younger Athabasca and
Kombolgie basins have been intensively studied (e.g. Hoeve and Sibbald, 1978; Wilson and
Kyser 1987; Kotzer and Kyser, 1995; Sweet et al., 1999; Kyser et al., 2000; Polito et al.,
2004; Alexandre et al. 2007; Cuney and Kyser, 2008). Although deposits associated with
successor basins in the Beaverlodge and South Alligator River areas were extensively
explored in the 1950s, only limited research on their genesis has been published (e.g.
Robinson, 1955; Koeppel, 1968; Beck, 1969; Sassano et al., 1972; Tremblay, 1972; Hoeve,
1981; Johnston, 1984; Needham, 1985; Sibbalt, 1985; Rees, 1992). Therefore, the key
1

processes by which these deposits formed remain a contentious issue. Their timing and
genetic relationships with the unconformity-type deposits in the younger U-rich Athabasca
and Kombolgie basins, and the successor basins themselves, are inconclusive. An
understanding of the structural and geological setting, timing, origin, and nature of the
fluids that formed them and altered them and their relationship with the younger
unconformity-type uranium deposits are necessary to establish a more definitive genetic
model for the formation of these deposits and to contribute to more effective exploration
strategy in successor and associated basins in general.
This thesis reflects results of a study on the fluid evolution and structural control on
uranium deposits in the Martin Lake Basin in the Beaverlodge area, Northern
Saskatchewan, Canada, and the El Sherana Basin in the South Alligator River area,
Northern Territories, Australia, using modern geochemical techniques integrated with
detailed structural analysis. Results are compared to existing models for uranium deposits
in the younger Athabasca and Kombolgie basins.
1.1 Geological setting of the Beaverlodge area
1.1.1. Regional geological and structural setting
The Beaverlodge area lies in the southwestern Rae province of the Churchill
province, which is located in the northwest section of the North American shield (Fig. 1.1).
The Churchill province is subdivided into the Rae and Hearne domains separated by the ca.
1.91-1.90 Ga Snowbird Tectonic Zone (Hoffman, 1990; Hanmer et al., 1995) and bordered
to the northwest by the ca. 1.99-1.92 Ga Taltson-Thelon Orogen (Thériault, 1992; McNicoll
et al., 2000) and to the southeast by the ca. 1.9-1.8 Ga Trans-Hudson Orogen (Ansdell and
2

Yang, 1995). The Beaverlodge area comprises Archean to late Paleoproterozoic rocks that
can be broadly divided into four packages:
3

Figure 1.1. Generalized geological map of the Western Churchill province, Canada showing
the location of the Beaverlodge area (modified from Davidson and Gandhi, 1989).
(1) Archean (ca. 3 Ga) basement granitoid and gneiss (Hartlaub et al., 2006);
(2) Variably deformed and metamorphosed Neoarchean to Paleoproterozoic (ca. 2.33 Ga
to 2.1 Ga) Murmac Bay Group rocks (Hartlaub and Ashton, 1998; Hartlaub et al.,
2004a; Knox et al., 2007, 2008) that unconformably overlie the basement rocks. This
Group contains quartzite, dolostone, psammite, iron formations, mafic rocks, and pelite
(Hartlaub and Ashton, 1998; Ashton et al., 2000). Deposition of the Murmac Bay
Group was synchronous with intrusion of the ca. 2.33 Ga to 2.29 Ga North Shore
Pluton suite (Ashton and Hunter, 2003) including the 2321±3 Ma Gunnar granite
(Hartlaub et al., 2004a), which hosts a major U deposit (Ahston et al., 2010; Dieng et
al., 2011).
(3) Paleoproterozoic ca. 1820 Ma siliciclastic red-bed sedimentary rocks and associated
alkaline volcanic rocks of the Martin Lake Basin (Langford, 1981; Mazimhaka and
Hendry, 1983; Hendry, 1985; Morelli et al., 2009), which unconformably overly the
granitic basement and Murmac Bay Group rocks;
(4) late Paleoproterozoic ca. 1750-1720 Ma sedimentary rocks of the Athabasca Group
(Sibbald, 1983; Kyser et al., 2000; Rainbird et al., 2007) that unconformably overly
Martin Lake Basin rocks.
The basement granite and rocks of the Murmac Bay Group record the effects of
at least four major Paleoproterozoic thermotectonic events:
4

(1) the ca. 2.4-2.3 Ga Arrowsmith Orogen (Berman et al., 2005; Hartlaub et al., 2007;
Ashton and Hartlaub, 2008), interpreted as an extensional orogen associated with the
deposition of the Murmac Bay Group and the intrusion of the North Shore Plutons.
(2) the ca. 1.99-1.93 Ga Thelon-Taltson Orogen (McDonough et al., 2000; McNicoll et al.,
2000) produced NNE-directed recumbent folds (D 1/2 ) accompanied by ductile
transposition and superseded by upright NNW-trending folds (D 3 /F 3 ) (Bethune et al.,
2010). The deformation attained granulite-facies metamorphic conditions by ca. 1.93
Ga (Ashton et al., 2006, 2007). The Thluicho Lake Group (Hunter, 2007), a
greenschist-facies conglomerate-arkose-argillite succession basin located west of the
Beaverlodge area, was deposited between ca. 1.92 Ga and 1.82 Ga (Ashton et al.,
2009a) during the post-peak Taltson-Thelon Orogen.
(3) the ca. 1.91-1.90 Ga Snowbird Tectonic Zone (Baldwin et al., 2003; Bethune et al.,
2008; Ashton et al., 2009a) refolded D 1 to D 3 structures forming NE-trending,
predominantly SW-plunging F 4 folds (Ashton et al., 2007).
(4) the ca. 1.9-1.8 Ga east-west compressional regime of the Trans-Hudson Orogen formed
gentle, open north-trending folds (F 5 ) that are transected by a set northeast-trending
brittle fractures (Ashton et al., 2006, 2009b).
1.1.2. Uranium mineralization
The Beaverlodge area hosts numerous U deposits that are spatially associated with
the Martin Lake Basin (Fig. 1.1). These deposits were actively mined between 1953 and
1963. Ore grades were in the range of 0.15% U to 0.25% U but in places, up to 0.4% U
(Robinson, 1955). About 28,500 t U 3 O 8 was mined (Table 1.1; Sibbald and Quirt, 1987),
5

which is the equivalent of the Millennium deposit (Roy et al., 2005) in the Athabasca
Basin. The Ace-Fay and Gunnar deposits produced up to 80% of the total U ore (Table
1.1).
Deposits
Production (t U3O8)
Eldorado-Ace-Fay 19,232
Gunnar 6,892
Eldorado Verna- Bolger 7 63
Eldorado-Hab 436
Rix Smitty 295
Eldorado - Dubyna 251
Cinch Lake 197
Cayzor Athabasca 163
Lorado 89
Eldorado Eagle 77
Rix Leonard 41
Nicholson 41
National Exploration 3 0
Nesbitt Labine 23
Eldorado Fishhook 15
Eldorado Martin Lake 11
Uranium Ridge 10
Total Production 28,546
Table 1.1. Uranium production of the Beaverlodge area (after Sibbald and Quirt, 1987)
The uranium deposits were generally subdivided into pegmatite-type and vein-type
deposits (Beck, 1969; Robinson, 1955; Tremblay, 1972). The latter are further divided into
a small group of complex mineralogy and a larger group of simple mineralogy (Tremblay,
1972; Hoeve, 1978; Kotzer et al., 1995). Deposits of simple mineralogy consist of
pitchblende with lesser amount of pyrite, chalcopyrite, galena, ±nolanite and minor amount
of bornite, covellite, chalcocite, digenite, and native copper (Robinson, 1955). Deposits of
complex mineralogy consist of pitchblende with cobalt-nickel arsenides and sulfides,
cobalt-nickel lead selenides, and native platinum, gold, silver and copper in addition to
6

minerals found in deposits of simple mineralogy (Robinson, 1955). The ore is associated
with high Si, Al, Fe, Ca, Na, Cu, Pb and V (Beck, 1969) and the ore mineralogy is similar
to the complex-type unconformity-related U deposits in the Athabasca Basin (Hoeve et al.,
1978; Fayek et al., 1997). The common gangue minerals in order of abundance are
hematite, calcite, chlorite, quartz, feldspar and fluorite (Robinson, 1955).
Hoeve et al. (1978) proposed two different periods of metallogenesis based on a
correlation between deposit types and their timing. They argue that deposits of simple
mineralogy formed at 1780 Ma (Koeppel, 1968) and are associated with Na-metasomatism
during the peak Trans-Hudson Orogen, whereas those of complex mineralogy formed at ca.
1500-1400 Ma and may be equated to the unconformity-type deposit of diagenetic origin in
the Athabasca Basin (Peiris et al., 1988; Kotzer et al., 1990, 1993, 1995; Rees, 1992).
1.2. Geological setting of the South Alligator Mineral Field area
1.2.1. Regional geological and structural setting
The South Alligator River area is located in the South Alligator Valley, in Northern
Territories, Australia (Fig. 2.1). It comprises rocks aged from Neoarchean to late
Paleoproterozoic, which are divided into four main sequences:
(1) Neoarchean ca. 2.5 Ga basement granitic rocks (Needham and Stuart-Smith, 1985);
(2) Paleoproterozoic (ca. 2.2 Ga to 1.87 Ga) metasedimentary and metavolcanic rocks of
the Pine Creek Orogen sequence unconformably overlying basement rocks (Page et al.,
1980; Needham et al., 1987). In the South Alligator River area, the upper part of the
South Alligator Group, the Koolpin Formation is a succession of interbedded siltstone,
7

dolostone and carbonaceous shale (Lally et al., 2006) that host most of the uranium
mineralization (Valenta, 1989, 1991; Wyborn et al., 1991; Mernagh et al., 1994; Lally
and Bajwah, 2006);
8

Figure 1.2. Generalized regional geology of the Pine Creek Inlier, showing uranium fields,
deposits, and prospects (modified from Needham et al., 1988).
(3) Paleoproterozoic (ca. 1829 Ma to 1822 Ma) silisiclastic red beds and associated felsic
and mafic volcanic rocks of the El Sherana-Edith River Group unconformably overlie
Pine Creek Orogen sedimentary rocks (Jagodzinski, 1992; Kruse et al., 1994); and
(4) Late Paleoproterozoic (ca. 1822 Ma to 1720 Ma) volcanic and sedimentary rocks of the
Kombolgie Basin (Sweet et al., 1999) unconformably overlying older rocks and are
intruded by the 1723±6 Ma Oenpelli dolerite (Kyser et al., 2000).
Johnston (1984) and Valenta (1990) described three deformation phases in the South
Alligator River area, which are related to the ca. 1.87-1.78 Ga Top End Orogen (Needham
and DeRoss, 1990). D 1 deformation occurred during the ca. 1.87-1.96 Ga Barramundi
Orogen (Page and Williams, 1988) and produced isoclinal folding and bedding-parallel
cleavage, related to major low-angle reverse faulting, particularly at the base of the Koolpin
Formation (Johnston, 1984). D 2 occurred during the 1.86-1.84 Ga Nimbuwah event
(Ferguson and Needham, 1978; Lally and Worden, 2004) and formed regional-scale,
northwest trending, upright, tight to isoclinal folds and a penetrative axial-plane cleavage.
This event is associated with greenschist grade metamorphism in the South Alligator River
area. Post-Nimbuwah D 3 deformation is characterized by open, upright northeast-trending
folds and affected the El Sherana Basin rocks (Valenta, 1991).
1.2.2. Uranium mineralization
U mineralization occurs in three main areas of the Pine Creek Orogen: the Alligator
Rivers Uranium Field, the South Alligator Rivers Uranium Field, and the Rum Jungle
9

Mineral Field (Figure 1.2). Many deposits in these areas are classified as unconformity-type
(Lally et al., 2006). In the South Alligator Rivers area, U deposits lie within a northwesttrending
structural belt of Paleoproterozoic metasedimentary and metavolcanic rocks
(Walpole et al. 1968; Crick et al. 1980; Needham et al. 1988; Valenta, 1991; Wyborn et al.
1990a). Thirteen deposits (Table 1.2) and fifteen prospects were discovered by 1953
(McKay and Miezitis, 2001). Between 1956 and 1964, a total of 875 t of U 3 O 8 from 146
500 t of ore was produced (Table 1.2, Fisher, 1968). The bulk of the production was from
underground operations, with a few small open-cut pits (Lally et al., 2006).
Deposits Ore tonnage Grade t U 3 O 8 Au and PGE
Coronation Hill (production and reserve) 0.363 Mt 0.52 1869 19.6t Au, 0.8t Pt, 2.1t Pd
El Sherana (production) 41100t 0.55 226 Minor Au
El Sherana West (production) 21658t 0.82 185 Minor Au
Rockhole (production) 13155t 1.11 152 Minor Au
Palette (production) 4850t 2.46 124
Saddle Ridge (production) 30341t 0.24 78
Scinto 5 (production) 5800t 0.37 22
Scinto 6 (production) 1760t 0.16 3
Koolpin Creek (production) 530t 0.13 3
Skull (production) 630t 0.55 3
Sleisbeck (production) 0.34 3
Table 1.2. Production for U deposits in the Northern Territory, after Fisher, 1968.
Most of the deposits lie on or near the El Sherana–Palette fault (Fig. 1.2), a
northwest-striking dextral strike-slip fault system (Valenta, 1990), and were formed in
dilatational zones at fault bends or intersections (Valenta, 1991). The deposits occur in
greenschist facies host rocks and are surrounded by alteration zones that may extend for
over 1 km (Mernagh et al., 1994). The mineralization is essentially uraninite associated
with precious metals occurring as vein-type lodes in faults or shears, and occurs at the
unconformity between sediments of the El Sherana Group and the underlying cherty
10

ferruginous siltstone of the Koolpin Formation (Ayres et al., 1975). The U mineralization is
accompanied by minor amount of galena, chalcopyrite, pyrite, native gold, and clausthatite
(Ayres et al., 1975). The syn-ore alteration is characterized by muscovite-chlorite
±hematite±kaolinite±biotite (Wyborn, 1992; Mernagh and Wyborn, 1994).
1.3. Uranium mineralized systems in the Athabasca and Kombolgie basins
Uranium deposits in the Athabasca and Kombolgie basins are major sources of high
grade U ore (McGill et al., 1993; Bruneton, 1987). These deposits consist of massive pods,
veins and disseminations of uraninite spatially associated with unconformities between
basement Paleoproterozoic metasedimentary and Archean to Paleoproterozoic granitoid
rocks and overlying relatively flat-lying, late Paleoproterozoic siliciclastic fluvial red-bed
strata (Hoeve and Sibbald, 1978; Hoeve and Quirt, 1984; Wallis et al., 1986; Sibbald and
Quirt, 1987).
The uranium deposits can be hosted in structures in the basement (ingress type, Fig.
1.3) or in the overlying siliciclastic strata and paleo-weathered basement rocks (egress type,
Fig. 1.3) at the unconformity (Hoeve et al., 1984; Sibbald, 1985; Fayek and Kyser, 1997).
The ore-forming fluids originate either from the overlying sandstone (e.g. Kotzer et al.,
1995; Polito et al., 2005; Cuney and Kyser, 2008) or the underlying basement (e.g. Cuney
et al., 2005). These deposits are associated with alteration zones around the mineralization
(Hoeve et al., 1984; Quirt, 2003). In basement-hosted deposits, illitization is predominant in
the distal alteration zone from the U mineralization, and chloritization is the typical
alteration in the proximal zone (e.g. Wilde, 1989; 1992; Kotzer et al., 1995; Polito et al.,
11

2005). U mineralization is controlled by structures that have been reactivated, which are
favorable sites for fluid circulation (Schultz, 1991; Tourigny, 2002).
Fracture-Controlled
Mobilized U Mineralization
(Perched)
Lake
U Mineralization
at unconformity
(Basin-hosted)
Unconformity
Pelitic
Gneiss
Vein & Breccia
U mineralization
basement-hosted
Pelitic
Gneiss
Granitic
Gneiss
Graphitic
Pelitic Gneiss
Arkosic
Gneiss
Quartzite
Figure 1.3. Genetic model for unconformity-type U deposit (modified from Cuney and
Kyser, 2008).
Unconformity-type U deposits in the Athabasca and Kombolgie basins formed at ca.
1600 Ma and 1675 Ma, respectively, (Alexandre et al., 2006; Polito et al., 2012).
Temperatures were 200 o C and involved the interaction of oxidizing, saline basinal fluids
carrying U 6+ with either reducing basement rock types (basement-hosted, Fig. 1.3) or
reducing fluids from the basement (sediment-hosted, Fig. 1.3), thereby precipitating U 4+ at
the unconformity (e.g. Hoeve and Quirt, 1984; Kotzer and Kyser, 1995; Cuney et al.,
2005). Unconformity-type U deposits in the Athabasca and Kombolgie basins have
produced up to 35% of the world U production (e.g. Ruzicka, 1996; Ghandi, 2007),
12

compared to the small percentage produced in successor basins (Table 1.3) (Sibbald and
Quirt, 1987).
ore (Kt) % U Tonnes U
Olympic Dam (Australia) 2877610 0.03 863283
Athabasca Basin (Canada) 28810 1.922 553778
Kombolgie Basin (Australia) 87815 0.323 283304
Thelon Basin (Canada) 11989 0.405 48510
Beaverlodge District (Canada) 15717 0.165 25539
Hornby Bay Basin (Canada) 900 0.3 2700
South Alligator Valley U Field - 0.66 2668
Paterson Terrane (Australia) 122200 0.25 30
Table 1.3. Amount of U resources and average grades (modified from Jefferson et al., 2007).
Uranium also occurs in other deposit types (Fig. 1.4) including: breccia complex,
sandstone hosted, surficial, conglomeratic, volcanic, metasomatic, metamorphic, granitehosted,
and vein-type deposits (Cuney and Kyser, 2008). So far, unconformity-related
deposits have produced the majority of U (Table 1.4).
13

Figure 1.4. Schematic representation of the location of various types of U deposits (modified
from Cuney and Kyser, 2008)
U deposit type Global U production (%) Global U resource (%)
Unconformity-related 42 4
Sandstone-hosted 30 10
Metasomatic 9 4
Volcanic 9 1
Breccia Complex 8 6
Quartz-pebble conglomerate 2 2
Table 1.4. Global U production and resources by deposit type (after Cuney and Kyser 2008).
1.4. Uranium mineralized systems in the successor basins
In successor basin areas, there is no consensus regarding the origin of the fluids that
carried the uranium, the timing of the deposits or their relationship with the younger U-rich
Athabasca and Kombolgie basins primarily because they are wholly understudied. Previous
results on deposits in successor basins are discussed in chapters 2 to 4. Diagenetic
processes and fluid evolution in the Martin Lake and El Sherana basins have never been
fully addressed, nor has basin versus basement sources for U and other metals in the
deposits. More recent studies on U in successor basins focussed only on aspects of a few
deposits and the older studies dating back to the 1950’s often lacked the necessary details
and technologies needed to construct meaningful exploration models (e.g. Condon and
Walpole, 1955; Tremblay, 1972). Indeed, there is a lack of basic knowledge on whether the
successor basins could form or host an exploitable deposit and what their significance is to
the overlying U-rich Athabasca and Kombolgie basins.
14

1.5. Purpose of this Thesis
The main objectives of this thesis are:
(a) to re-evaluate the character and formation of uranium deposits in successor basins in
Canada and Australia and compare them to those in the younger U-rich basins with
which they are spatially associated, and
(b) to identify key factors controlling U mineralization in successor basins by integrating
aspects of structural geology, geochronology, petrography and geochemistry (Fig. 1.5)
to detail the structural and fluid evolution of uranium deposits in successor basins and
how they are related to unconformity-related U deposits in the younger basins.
Figure 1.5. Geological disciplines used in this study to evaluate the character and formation of
uranium deposits in successor basins including deformation that created fluid conduits,
timing of the fluids events, the nature of the ore-forming fluid and the uranium source. All are
necessary to construct a conceptual genetic model for uranium deposit.
15

In particular, the key issues to be addressed include:
(1) The geological and structural settings of these deposits. The goals are to define the
deformation history and to analyze the geometry and kinematics of uranium-bearing
structures that are necessary to understand key structural features that are favorable for
fluid mobility and uranium mineralization (Fig. 1.5).
(2) The paragenesis and crystal chemistry of the alteration assemblages and uranium
mineralization in successor basins (Fig. 1.5), including ore and alteration mineral
assemblages and their relative timing.
(3) Determination of the age, origin, composition and timing of the fluids that produced
the uranium mineralization in successor basins (Fig. 1.5). Results are compared with
fluids that formed the younger unconformity-type U deposits.
(4) Establish a conceptual genetic model for uranium mineralization in successor basins by
integrating results from structural, geochronological, petrographic and geochemical
data (Fig. 1.5) and predict sites of mineral deposition in analogous successor basins by
identifying key fluid and deformation events in their evolutions that are linked to
economic uranium mineralization.
This study focuses on uranium deposits in the Beaverlodge (Fig.1.1) and South
Alligator River areas (Fig. 1.2). These two areas share similar geological and structural
setting. They host older U deposits in Paleoproterozoic successor basins that are spatially
associated with unconformity-type U deposits in younger late Paleoproterozoic basins. In
the Beaverlodge area (Fig. 1.1), the Gunnar, Ace-Fay, and Cinch Lake deposits are studied.
These deposits represent the spectrum of deposit types and are the largest in the area (Table
16

1.1). In the South Alligator Valley area, research is focused on the Coronation Hill and El
Sherana deposits, the largest deposits of their type in the area (Fig. 1.2, Table 1.2).
1.6. Thesis Structure
The results of this research are presented in three manuscripts (Chapters 2 to 4).
Chapter 2 (accepted pending moderate revisions in Precambrian Research) details
the timing of deformation, fluid flow and uranium mineralization in the Beaverlodge area.
U-Pb geochronology of uraninite from various uranium deposits, together with
petrographic and structural analysis along the Main Ore shear zone at the Cinch Lake
deposit and the Saint Louis fault at the Ace Fay deposit, are used to constrain the timing of
deformation and fluid events and to clarify the relationship between fault activity and
uranium mineralization. Ages of the uranium mineralization and late alteration events that
affected them are used to correlate the chronology of fault activity and uranium
mineralization to major thermotectonic events associated with the evolution of the North
American shield.
Chapter 3 (accepted pending moderate revisions to Economic Geology) evaluates the
character and formation of the fluids that formed uranium deposits in the Beaverlodge area
and determines key geochemical factors that control uranium mineralization. A mineral
paragenesis that details the relative timing of alteration minerals is presented. Stable isotope
geochemistry, rare earth element contents in uraninite and mineral crystal chemistry are
used to constrain the nature and origin of fluids. These results are used to identify key
factors controlling uranium mineralization in deposits of the Beaverlodge area, present a
17

genetic model for the U mineralization, and compare the Beaverlodge U deposits to those
in the younger, U-rich Athabasca Basin.
Chapter 4 (submitted to Mineralium Deposita) focuses on U deposits in the South
Alligator Valley area. In this chapter, we evaluate the character and formation of U
mineralization of the El Sherana and Coronation Hill deposits using a mineral paragenesis
that details the relative timing of alteration minerals. We also constrain the timing, nature
and origin of the fluids in equilibrium with these minerals using stable isotope
geochemistry, U-Pb geochronology of paragenetically well-characterized U-rich minerals,
and mineral crystal chemistry. These results are used to identify key processes controlling
U mineralization in the South Alligator Valley area, present a genetic model for the U
mineralization, and compare the South Alligator River U deposits to those in the younger
and U-rich Kombolgie Basin.
18

CHAPTER 2
TECTONIC HISTORY OF THE NORTH AMERICAN SHIELD
RECORDED IN URANIUM DEPOSITS IN THE BEAVERLODGE
AREA, NORTHERN SASKATCHEWAN, CANADA
Abstract
Paragenetic and structural relationships and geochronology of minerals in uranium
deposits in the Beaverlodge area, Northwestern Saskatchewan, Canada, reveal six periods
of uranium mineralization associated with multi-stage deformation during the Proterozoic.
The Saint Louis fault and the Main Ore shear zone are northeast striking, southeast-dipping,
oblique-normal and dextral fault systems that have mylonite-dominated footwalls. These
faults display evidence of exhumation and episodic structural reactivation at progressively
shallower crustal levels, accompanied by fluid flow, hydrothermal alteration, and uranium
mineralization.
New geochronologic data on uranium mineralization and alteration events record
over 2.3 Gyrs of protracted tectonic evolution of the North American shield. 207 Pb/ 206 Pb
ages of 2293±17 Ma and 2289±20 Ma date two minor uranium mineralization stages
associated with cataclasite rocks and early tensional veins, respectively, coincident with
late Arrowsmith orogenic exhumation. Following emplacement of the Gunnar granite at
2321±3 Ma, albite metasomatic alteration of the granite is associated with a third moderate
uranium mineralizing event. During the late Paleoproterozoic, exhumation along major
faults caused the deformation style to change from dominantly brittle-ductile to brittle at
shallower structural levels. Massive brecciation of pre-existing rocks is associated with the
19

fourth and most significant uranium-mineralizing event at 1848±5 Ma, coincident with fault
reactivation during tectonic shortening and regional metamorphism related to the Trans-
Hudson Orogen or more likely post-peak compressional uplift during terminal collision of
the Taltson-Thelon Orogen. Subsequently, formation of the Martin Lake Basin and
intrusion of mafic dikes are related to the fifth minor uranium mineralizing event at
1812±15 Ma reflecting rifting related to late stage Trans-Hudson Orogen. Late mineralized
veins during the Mesoproterozoic crustal growth of the Nuna supercontinent are associated
with the sixth mineralizing event at 1620±4 Ma, coincident with the Mazatzal Orogen and
the formation of the unconformity-related uranium mineralization in the proximal
Athabasca Basin.
Post-mineralization alteration and resetting events of uraninite further record various
major orogenic events that have affected the North American shield.
2.1. Introduction
Deeply exhumed fault zones can serve as vehicles to understand the complex timing
relationships between deformational, hydrothermal and ore-forming processes. An
important step in understanding the structural setting of uranium deposits associated with
highly and multiply deformed and metamorphosed Paleoproterozoic terranes is establishing
the timing relationships of fault activity and uranium mineralization to regional
thermotectonic events.
The Beaverlodge area in the central-southern Archean Rae province, Northwestern
Saskatchewan, Canada (Fig. 2.1), hosts numerous fault-controlled uranium deposits. The
Main Ore shear zone at the Cinch Lake deposit and the Saint Louis fault at the Ace-Fay-
20

Verna deposits are two northeast-striking, southeast-dipping, oblique-normal and dextral
fault systems that offer an excellent setting to understand the temporal relationship of fault
activity and uranium mineralization to regional thermotectonic events (Fig. 2.2).
The timing and tectonic setting of uranium mineralization in the Beaverlodge area has
been a contentious issue. Although the spatial relationship between uranium mineralization
and major structures has been well documented (e.g. Robinson, 1955; Tremblay, 1968;
Beck, 1969; Beecham, 1969; Morton and Sassano, 1972; Sassano, 1972; Sibbald, 1982,
Ashton et al., 2000, 2010), the timing of tectonic and fluid events in these deposits and their
relationships with fault activity and regional thermotectonic events have never been fully
elucidated.
In this chaper, U-Pb dating by laser ablation-high resolution inductively-coupled
plasma mass spectrometry (LA-HR-ICP-MS) on uraninite from uranium deposits, together
with petrographic and structural analysis along the Main Ore shear zone and the Saint Louis
fault, are used to constrain the timing of deformation and fluid events and to clarify the
relationship between fault activity and uranium mineralization. Ultimately, ages of primary
uranium mineralization and late alteration events that affected them are used to correlate
the chronology of fault activity and uranium mineralization to major orogenic events
associated with the evolution of the North American shield.
2.2. Geologic Setting
2.2.1. General geology
21

The Beaverlodge area is part of the Churchill province, which is located in the
northwest section of the North American shield (Fig. 2.1). The Churchill province is
subdivided into the Rae and Hearne domains separated by the ca. 1.91-1.90 Ga Snowbird
Tectonic Zone (Hoffman, 1990; Hanmer et al., 1995) and bordered to the northwest by the
ca. 1.99-1.92 Ga Taltson-Thelon Orogen (Thériault, 1992; McNicoll et al., 2000) and to the
southeast by the ca. 1.9-1.8 Ga Trans-Hudson Orogen (Ansdell and Yang, 1995). The
Beaverlodge area lies within the southwestern Rae province (Fig. 2.1) and comprises
Neoarchean to Mesoproterozoic rocks that can be broadly divided into four packages (Fig.
2.2): (1) Neoarchean basement granitoid and gneiss (Hartlaub et al., 2006); (2) variably
deformed and metamorphosed Neoarchean to Paleoproterozoic Murmac Bay Group rocks
(Hartlaub and Ashton, 1998; Hartlaub et al., 2004a) that uncomformably overlie the
basement rocks; (3) Paleoproterozoic siliciclastic red-bed sedimentary rocks and associated
alkaline to sub-alkaline volcanic rocks known as the Martin Lake Basin (Hendry, 1983;
Morelli et al., 2001, 2009). Martin Lake Group basal conglomerates directly overlie
quartzites of the Murmac Bay Group and argillaceous rocks of the Thluicho Lake Group
(Scott, 1978, Hunter et al., 2003, 2004; Yeo, 2005) at angular unconformities in the western
Beaverlodge Domain and along the northern shore of Lake Athabasca, respectively (Ashton
et al., 2009), and (4) Mesoproterozoic sedimentary rocks of the Athabasca Group (Rainbird
et al., 2007) that uncomformably overlie Martin Lake Basin rocks.
The basement complex comprises a number of granitoids including the Elliot Bay
(3014±10 Ma; Persons, 1983), Lodge Bay (3060±40 Ma; O’Hanley, et al., 1991), and
Cornwall Bay (2999±7 Ma; Hartlaub et al., 2004a) granites. The unconformity between the
22

asement and the Murmac Bay Group is generally sheared but the basal polymictic
conglomerate is locally preserved (MacDonald and Slimmon, 1985).
Location Map
Study area
Uranium deposits
Figure 2.1. Simplified geological map of the southwestern Churchill province, Canada,
showing lithotectonic units, uranium deposits and the Beaverlodge location. (modified from
Hoffman, 1988).
The Murmac Bay Group is composed of metamorphosed and moderately to highly
deformed basal quartzite, basalt, ultramafic to intermediate igneous rocks, psammite and
pelite, with minor amounts of conglomerate, banded iron formation, and carbonates
(Hartlaub and Ashton, 1998; Ashton et al., 2000). The Group is metamorphosed from
lowermost amphibolite to granulite facies to lower greenschist facies (Ashton and Card,
23

1998; Hartlaub and Ashton, 1998). Recent work indicates that the basal quartzo-feldspathic
units have a maximum depositional age of 2330±3 Ma (Card et al., 2007). The Murmac
Bay Group is intruded by a suite of ca. 2.33–2.30 Ga granites named ‘North Shore Plutons’
(Macdonald et al., 1985) including the 2321±3 Ma Gunnar granite (Hartlaub et al., 2007),
which hosts the Gunnar uranium deposit (Fig. 2.2). The timing of deposition of the
Murmac Bay Group with respect to emplacement of the ‘North Shore Plutons’, thought to
be related to the Arrowsmith Orogen (Hartlaub et al., 2007), remains contentious.
The Paleoproterozoic Martin Lake Basin (Fig. 2.2) is estimated to be a ca. 5000 m-
thick, molasse, red-bed succession (Langford, 1981; Mazimhaka and Hendry, 1984) of
essentially unmetamorphosed arkose, conglomerates, and siltstone with mafic flows and
sills of alkaline affinity (Morelli et al., 2009). The fault-controlled basin is confined to a
broad open syncline centered about the Martin Lake (Ramaekers, 1981; Ashton et al.,
2001). Suites of east to southeast striking mafic dikes, dated at 1818±4 Ma, are interpreted
as feeders to the Martin Lake mafic flows (Morelli et al., 2009). The Martin Lake Basin
formed during a late phase of the Trans-Hudson Orogen and can therefore be classified as
a successor basin (Clendenin et al., 1988).
Outliers of the Athabasca Formation lie above the Martin Lake Basin south of the
Beaverlodge area (Fig. 2.2), where they generally comprise flat-lying and undeformed
sandstone with minor mudstone, conglomerate and greywacke (Sibbald, 1983).
24

Strike slip normal fault
Figure 2.2. Simplified geological map of the Beaverlodge area and location of uranium
deposits, including those in this study. (modified from Macdonald and Slimmon, 1985).
Rocks within the Beaverlodge area have been affected by at least four episodes of
deformation (Bethune et al., 2008; Ashton et al., 2009a). The first deformation episode
25

(D 1 ) produced a regional migmatitic foliation (S 1 ). The second deformation episode (D 2 )
produced tight to isoclinal folds of early S 1 fabric and associated shear zones (Ashton and
Hartlaub, 2008). These two deformational events resulted in an east-southeast striking
structural fabric coinciding with the 1.94-1.92 Ga peak metamorphism of the Taltson
Magmatic Suite (McDonough et al., 2000). An overprinting northeast-striking regional
fabric associated with tight to isoclinal foldind (D 3 ) is interpreted to be synchronous with
the 1.91-1.90 Ga metamorphic event of the Snowbird Tectonic Zone (Bethune et al.,
2008). Gentle upright folds with north-trending hinges represent the last phase of regional
deformation (D 4 ) that affected the Martin Lake Basin and Murmac Bay Group rocks; these
are likely associated with late stage of the Trans-Hudson Orogen (Ashton et al., 2009a).
2.2.2. Previous models age for uranium mineralization in the Beaverlodge area
The Beaverlodge area hosts a multitude of uranium deposits (Fig. 2.2), which were
actively mined between 1953 and 1963. About 284 deposits were known by 1969 and ca.
25000 tU was mined (Sibbald and Quirt, 1987). Ore grades were in the range of 0.15 to
0.25% U, but in places, up to 0.4% U (Robinson, 1955).
The age and evolution of the uranium mineralization in the Beaverlodge area are
debated and different age models have been proposed. Collins et al. (1954) suggested that
the first period of uranium mineralization lasted from 1860 to 1630 Ma with alteration
occurring at 1100-900 Ma, 650-600 Ma, and 400-300 Ma. They interpreted this range of
ages as related to alteration and resetting stages during successive tectonic events.
Robinson (1955a) indicates that the earliest vein-type uranium mineralization occurred
between 1600 Ma and 1500 Ma and followed, possibly transitionally, earlier deposition of
26

U and Th in syngenetic deposits. He suggested that the vein-type deposits were followed
by periods of mineralization in the intervals of 1500-1400 Ma, 950-850 Ma, and 350-250
Ma and indicates that these deposits were reopened and reworked over a long period of
time. Wasserburg and Hayden (1955) obtained an age of ca. 1.87 Ma in uraninite from
Viking Lake deposit located east of the Ace-Fay deposits and interpreted this age as the
earliest uranium mineralization in the Beaverlodge area. Aldrich and Wetherill (1956) and
Eckelman and Kulp (1957) proposed that the uranium mineralization was deposited at
1900 Ma with subsequent alteration and Pb loss occurring at 1200 Ma and 200 Ma. Russel
et al. (1957) reported an age of 1800 Ma for the west orebodies of the Ace deposit (Fig.
2.2) and a second generation of mineralization at ca. 940 Ma. Results from Koeppel (1969)
support the formation and evolution of the uranium mineralization during five discrete
periods that span a time of more than 2200 Myr. Koeppel (1969) reported an U-Pb
concordia upper intercept age of 1930 Ma and a lower intercept of 1780 Ma with episodic
Pb loss at 1110 Ma, 270 Ma, and 200-0 Ma. He interpreted the age of 1930 Ma was related
to pegmatite-type mineralization and the 1780 Ma date as the age of the vein-type uranium
mineralization. Bell (1981) proposed an age of 1740 Ma for initial uranium deposition and
Dudar (1982) found apparent 207 Pb/ 206 Pb ages ranging from 1100 Ma to 430 Ma for
brannerite in the Fay deposit (Fig. 2.2). Interpretation of fluid inclusions, stable isotope,
and radiogenic isotope data from the veins and mine granites (Fig. 2.2) in the Goldfield
area, led Rees (1992) to identify up to six fluid events occurring from ca. 2.0 Ga to 1.0 Ga
that he interpreted to be related to major thermotectonic events.
27

These previous age models do not take into account the various styles of uranium
mineralization and associated deformation, and their spatial and relative temporal
relationships (Collins et al., 1954; Robinson, 1955a; Koeppel, 1969). Most of these models
have been limited to a single deposit (Russel et al., 1957; Bell, 1981; Dudar, 1982; Rees,
1992) that cannot provide a regional picture of the timing of uranium mineralization and
fluid events and their relationship to deformational history.
In this chapter, structural, petrographic and metamorphic relationships along the
Main Ore shear zone at the Cinch Lake deposit and the Saint Louis fault at the Ace-Fay-
Verna deposits (Fig. 2.2) are used to constrain the timing of deformation and fluid events.
Paragenetically constrained uraninite grains collected from five uranium deposits (Fig. 2.2)
are dated to determine the timing of the uranium mineralization and alteration events.
2.3. Methodology
2.3.1. U-Pb dating of uranium-rich minerals by LA-HR-ICP-MS
U-Pb isotope ratios were determined by laser ablation-high resolution inductivelycoupled
plasma mass spectrometry (LA-HR-ICP-MS) (Chipley et al., 2007) using a
Finnigan MAT ELEMENT XR HR-ICP-MS and a NEPTUNE HR-MC-ICP-MS, both
equipped with a high-performance Nd:YAG New Wave UP-213 laser ablation system at
the Queen’s Facility for Isotope Research. Ablation of uraninites was achieved on polished
thin sections using a 30 to 40μm spot size with 35% to 40% laser power at a frequency of
2Hz. The argon gas flows were as follows: cooling gas, 1.5l/min; auxiliary gas, 1.0l/min;
and sample carrier gas, 1.0 l/min. A low resolution of 350 (defined as the ratio of mass
over peak width mass at 5% of the signal height) was used. For each sample, 204 Pb, 206 Pb,
28

207 Pb, 235 U and 238 U were measured and corrections for common Pb were made scan-byscan
to each spot. No corrections were made to the 238 U/ 235 U ratios as they were near the
137.8 natural ratios. The ages were verified using an in-house 1000 Ma uraninite standard.
2.3.2. Electron-microprobe procedure and calculations of chemical Pb age of the
uranium mineralization
Polished thin sections were examined with reflected light optical microscopy and
Scanning Electron Microscopy. A Cameca SX-100 Electron Microprobe equipped with 4
wavelength-dispersive spectrometers, an EDS system, and Back-Scattered Electron and
Secondary-Electron Detectors at the University of Manitoba, Winnipeg, Canada, was used
to measure UO 2 , SiO 2 , CaO, Fe 2 O 3 , TiO 2 , Cr 2 O 3 , V 2 O 5 , PbO, P 2 O 5 , K 2 O ThO 2 , MnO,
Y 2 O 3 , Tb 2 O 3 , and CuO. Analytical results are accurate to 2% relative for major elements
and 5% relative for minor elements (

the age when the concentrations of the secondary elements (e.g. Ca, Fe and Si) were
negligible (e.g. Alexandre and Kyser, 2005).
Mineral name abbreviations used in this chapter are those from Kretz (1983). The
superscript numerical value on mineral name abbreviations reflects mineral growth stages.
2.4. Results
2.4.1. The Main Ore shear zone
2.4.1.1. Geology of the Cinch Lake deposit
The Cinch Lake deposit is located 2.5 km south of Uranium City (Fig. 2.2). The
uranium mineralization is hosted in quartzo-feldspathic gneiss (Turek, 1962; Tortosa,
1983) and associated with a northeast-striking band of mylonite named the Main Ore shear
zone, which parallels the Black Bay fault (Bergeron, 2001). Three main lithological units
outcrop in the Cinch Lake area that generally strike northeast and dip southeast: a
leucocratic porphyroclastic metagranitoid, a hornblende-feldspar gneiss, and a
melanocratic porphyroclastic metagranitoid (Fig. 2.3).
The leucocratic porphyroclastic metagranitoid unit is exposed in the southeastern
part and occupies the hanging wall of the shear zone (Figs. 2.3A and 2.3B). The rock is
cataclasite-dominated (Fig. 2.4A) weakly foliated and comprises broken fragments of
plagioclase, quartz and feldspar embedded in a matrix composed of hematite, quartz,
chlorite, calcite, sericite, and pyrite (Fig. 2.4B).
30

A
A’
B
31

Figure 2.3. A: Detailed geologic map of the Cinch Lake area showing main lithological units
and structural elements and B: Northwest-southeast geological cross-sections (line AA’)
across the Main Ore shear zone illustrating the listric oblique-normal and dextral sense of the
fault movement, location of the mylonitic and cataclasite portions of the fault zone and the
uranium mineralization intercepted in drill hole (see Appendix I for detailed structural
measurements and steroplots).
The leucocratic metagranitoid unit has a coarse-grained cataclasite texture in the
southeast part passing gradually into a fine-grained ultracataclasite texture toward the
northwest (Fig. 2.3).
The hornblende-feldspar gneiss outcrops within the fault zone (Fig. 2.3). The rock is
foliated, generally boudinaged, parallel to the dominant foliation (N240 o ) (Fig. 2.4C) and
composed of hornblende and feldspar porphyroclasts (Fig. 2.4D), which are locally
associated with biotite, chlorite, sericite, epidote and titanite.
The melanocratic porphyroclastic metagranitoid rocks are exposed northwest in the
footwall (Fig. 2.3). The unit is mylonite-dominated and consists of a mélange of
mylonitized metavolcano-sedimentary rocks (Figs. 2.4E and 2.4F), quartz-feldspar
mylonite (Figs. 2.4G and 2.4H) and boudinaged and foliated hornblende-feldspar gneiss.
32

Figure 2.4. Photographs of the three main lithostructural units: A: Field photo of the
cataclasite-dominated leucocratic porphyroclastic metagranitoid in the hanging wall of the
fault zone. B: Microphotograph of the cataclasite-dominated leucocratic metagranitoid
showing mylonite fragments and broken Kfs 1 and Qtz 1 grains embedded in a matrix of
crushed Kfs 1 , recrystallized Qtz 1 , and Src 2 and Py 2 . C: Field photo of the hornblende-feldspar
gneiss boudinaged and parallel to the foliation (N240 o ). D: Microphotograph of the
33

hornblende-feldspar gneiss showing Hbl 1 and Kfs 1 porphyroclasts. E: Field photo of the
mylonitized metavolcano-sedimentary rocks of the melanocratic metagranitoid unit. F:
Microphotograph of the mylonitized metavolcano-sedimentary rocks showing a mylonitic
fabric that consists of flattened and preferentially oriented trails of Bt 1 , Chl 1 , Src 1 ,
dynamically recrystallized Qtz 1 and rotated Kfs 1 porphyroclasts. G: Field photo of the
mylonitized quartz-feldspar rocks showing rotated δ- and σ-type winged Kfs 1 porphyroclasts.
H: Microphotograph of the mylonitized quartz-feldspar rocks showing σ-Kfs 1 , recrystallized
Qtz 1 and Src 1 . Pen indicates north. Bt: biotite, Chl: chlorite, Kfs: potassium feldspar, Hbl:
hornblende, Py: Pyrite, Qtz: quartz, Src: sericite.
2.4.1.2. Structural and metamorphic relationships in the Main Ore shear zone
The Main Ore shear zone records a complex history of ductile, brittle-ductile and
brittle deformation. The shear zone strikes N240 o and is steeply southeast dipping at the
surface (75 o to 85 o ) but becomes shallow at depth (30 o to 40 o ) (Fig. 2.3B). Southeast of the
shear zone, cataclasite and ultracataclasite dominate the hanging wall. The intensity of the
cataclasitic deformation increases from southeast to northwest toward the ductile shear
zone where the footwall is mylonite-dominated and overprinted by a mélange of
cataclasite, breccias and veins that host the uranium mineralization (Fig. 2.3B).
The ductile component of the shear zone defines the oldest deformation observed.
The shear zone displays a southeast dipping foliation and northeast trending elongation
lineation (Fig. 2.3) defined by elongate Kfs 1 feldspars and recrystallized Qtz 1 quartz (Fig.
2.4F). The mylonitic fabric is heterogeneously developed due to contrasting rheology of
the melanocratic metagranitoid rocks. The strain is more localized into relatively weak
rock types such as the metavolcano-sedimentary rocks (Fig. 2.4E), which have a mylonitic
fabric and foliation consisting of preferentially oriented trails of Bt 1 biotite, Chl 1 chlorite,
34

Ms 1 muscovite, Src 1 sericite, and dynamically recrystallized Qtz 1 quartz (Fig. 2.4F). The
quartzo-feldspathic mylonite exhibits recrystallized Qtz 1
quartz and Kfs 1 feldspars
porphyroclasts (Fig. 2.4H). Shear sense indicators such as δ and σ-type winged Kfs 1
feldspars porphyroclasts (Figs. 2.4G and 2.5A) and deflection foliation (Fig. 2.5B)
consistently display a dextral lateral sense of displacement.
The mylonitic foliation and lineation in the hornblende-feldspar gneiss contains the
higher metamorphic assemblage Kfs 1 +Pl 1 +Hbl 1 (Fig. 2.4D), compatible with amphibolite
facies metamorphism. Retrogression is indicated by partial replacement of Hbl 1 hornblende
by Bt 1 biotite along shear surfaces (Fig. 2.5C) and by replacement of Kfs 1 feldspars by Src 1
sericite (Fig. 2.5C). Bt 1 biotite is locally retrogressed into Chl 1 chlorite (Fig. 2.5D)
resulting in the mineral assemblage Bt 1 +Chl 1 + Src 1 +Qtz 1 typical of the greenschist
metamorphic facies. In places, Kfs 1 feldspars are completely sericitized and Chl 1 chlorite
completely replaced Bt 1
biotite, defining a lower greenschist metamorphic facies
(Qtz 1 +Src 1 +Hem 1 + Chl 1 ) (Fig. 2.5E). Late Chl 2 chlorite, Qtz 2 quartz, Ab 1 albite, Cal 1
calcite, and Ep 1 epidote veinlets cut the foliation. The mylonite is overprinted by a network
of ductile-brittle and brittle features.
Cataclasites occur in the hanging wall and in association with mylonites in the
footwall and are sub-parallel to the mylonitic fabric (Fig. 2.3). The cataclasite contains
variable-sized (0.2 to 0.5 mm) clasts of broken Qtz 1 quartz, Kfs 1 feldspars, and mylonite
fragments. The matrix is weakly foliated and contains recrystallized and milled Qtz 1
quartz, Cal 2 calcite, Chl 3 chlorite, Hem 3 hematite and Src 2 sericite (Fig. 2.5F). Sub-vertical
35

east-west striking en-échelon quartz-filled tension gashes indicate dextral lateral sense of
motion (Fig. 2.5G).
36

Figure 2.5. Various structural and textural relationships along the Main Ore shear zone at the
Cinch Lake deposit. A: Lateral dextrally rotated δ-type winged Kfs 1 porphyroclast in
melanocratic metagranitoid mylonite. B: Foliation deflection showing a dextral lateral sense
of shear. C: Hornblende-feldspar gneiss showing partial replacement of Hbl 1 by Bt 1 and Kfs 1
by Src 1 . D: Hornblende-feldspar gneiss showing partial replacement of Bt 1 by Chl 1 and Kfs 1
by Src 1 associated with Ttn 1 . E: Hornblende-feldspar gneiss in which Kfs 1 are completely
replaced by Src 1 and Bt 1 by Chl 1 . F: Cataclasite rock showing crushed mylonite fragments
37

and broken Kfs 1 and Qtz 1 embedded in a matrix of crushed and dynamically recrystallized
Qtz 1 . G: Sub-vertical northeast trending en-échelon Qtz-filled tension gashes showing dextral
lateral sense of displacement. H: Breccias with Cal 8 -filled matrix embedding angular
fragments of mylonite. I: Northeast-striking pegmatite dikes in the footwall of the shear zone.
J: Northeast-striking mafic dikes with chilled margin cross cutting the shear zone. K:
Northwest-striking breccia dikes comprising fragments of the host rock embedded in a Chlrich
matrix. L: Qtz veins Stockworks showing evidence of hydraulic fracturing. Pen indicates
north. Bt: biotite, Chl: chlorite, Hbl: hornblende, Kfs: Potassium feldspar, Qtz: quartz, Src:
sericite, U: uraninite.
Calcite-filled breccias overprint the mylonite and cataclasite rocks in the footwall of
the shear zone. Breccia fragments comprise angular mylonite and cataclasite clasts derived
from the host rock (Fig. 2.5H). The fragments vary in size from 0.2 mm to more than 2 cm.
The matrix is composed of Cal 8 calcite, Chl 7 chlorite and Hem 6 hematite (Fig. 2.5H).
Late brittle deformation features that overprint the shear zone include veins, dikes, joints,
and fractures. Field measurements indicate three set of steeply dipping joints striking
N320 o , N020 o , and N280 o .
Pegmatite dikes cut across the footwall of the shear zone. They strike northeast and
form a series of sheared elongate lenses of varying size (1 to 2m in length) and are
disrupted along the shear zone (Fig. 2.5I).
Diabase dikes form a swarm crosscutting all previous rocks. They are sub-vertical, weakly
deformed with chilled margins (Fig. 2.5J) and strike along two preferential directions:
parallel to the foliation and along the northwest striking pre-existing joints and fractures.
Breccia-dikes outcrop in the footwall of the shear zone (Fig. 2.5K) in three structural
sets of direction: N020 o , N090 o , and N320 o . The breccia-dikes vary in width from less than
38

1 cm to 10’s of cm. Fragments of the breccia are highly variable-sized (1 mm to 5 cm) and
consist of angular country-rock clasts embedded in a chlorite-rich matrix (Fig. 2.5K). The
contact between breccia-dikes and the host rock is sharp. A close spatial relationship is
observed between mafic dikes and breccia-dikes.
Late Chl 10 chlorite, Cal 11 calcite veins, and Qtz 5 quartz (Fig. 2.5L) crosscut all rock
types and are parallel to the set of joints.
2.4.2. The Saint Louis fault
2.4.2.1. Geology of the Ace-Fay-Verna deposits
The deposits are located along the Saint Louis fault (Fig. 2.2), which strikes
northeast and dips 50 o southeast (Fig. 2.6). The Ace and Fay ore bodies are located in the
footwall, whereas Verna is in the hanging wall. Sassano (1972) described four units that
host the uranium mineralization named the Fay Mine Complex comprising from oldest to
youngest: quartzite and conglomerates, phyllonite amphibolite, albite paragneiss and
granitic gneiss. These rocks overlie the Donaldson Lake and Foot Bay gneisses and are
uncomformably overlain by the Martin Lake basal conglomerates in the hanging wall of
the Saint Louis fault (Fig. 2.6).
2.4.2.2. Structural and metamorphic relationships in the Saint Louis fault
The Foot Bay gneiss, which occurs in the footwall and hanging wall of the fault (Fig.
2.6B) has a mylonitic texture characterized by rotated augen-shaped Kfs 1 feldspars
porphyroclasts (Fig. 2.7A) surrounded by recrystallized Qtz 1 quartz and layers of Chl 1
chlorite, Bt 1 biotite and Hbl 1 hornblende.
39

A
Meters
LEGEND
B
Figure 2.6. A: Detailed geologic map of the Ace-Fay-Verna deposits showing main lithological
units, structural elements and location of the uranium deposits (modified from Macdonald
40

and Slimmon, 1985) and B: NW-SE geological cross-sections across the Saint Louis fault (line
AA’) showing the geology, the trace of the Saint Louis Fault and the location of the uranium
mineralization (modified from Sassano, 1972).
The Donaldson Lake gneiss outcrops in the hanging wall and footwall of the fault
(Fig. 2.6B) and Sassano (1972) suggested that the Donaldson Lake gneiss is the cataclasite
equivalent of the underlying Foot Bay gneiss. The rock has a porphyroclastic texture
composed of Kfs 1 feldspars, Pl 1 plagioclase and Qtz 1 quartz scattered in a matrix of
recrystallized Qtz 1 quartz, crushed Kfs 1 feldspars and trails of Ms 1 muscovite and Chl 1
chlorite.
The quartzite occurs in the footwall (Fig. 2.6B) where it is mylonitized with strained
and recrystallized Qtz 1 quartz (Fig. 2.7B). Qtz 1 quartz grains are elongated and locally
wrapped by Src 1 sericite and Chl 1 chlorite. The mylonite is cut by Chl 2 chlorite and Src 1
sericite veinlets and overprinted by cataclasite with angular fragments of the mylonitized
quartzite occurring into the matrix (Fig. 2.7E).
The phyllonite amphibolite outcrops in the footwall, north of the Ace-Fay deposits.
In thin section, the rock shows symmetric crenulations that overprint the mylonitic fabric
(Fig. 2.7C). It is composed of alternating dark and light bands of Hbl 1 hornblende, Bt 1
biotite, Chl 1 chlorite, and Qtz 1 quartz, Kfs 1 feldspars and Src 1 sericite. In the amphibolite,
three fold phases (F1, F2 and F3) have been identified (Fig. 2.7D). F1 and F2 are isoclinal
recumbent folds having a dominant east-southeast axial plane foliation. Both F1 and F2 are
refolded by a north-northwest-trending open upright fold F3 producing a type 2
interference pattern (Ramsay, 1967). The amphibolite locally displays a breccia fabric with
mylonite fragments embedded in the matrix (Fig. 2.7H).
41

Figure 2.7. Microphotograph of various structural and textural relationships along the Saint
Louis fault at the Ace-Fay-Verna deposit. A: Rotated δ-type winged Kfs 1 porphyroclast in the
Foot Bay gneiss (sample is not oriented). The foliation is marked by train of Ms 1 , Src 1 , Chl 1 ,
recrystallized Qtz 1 and Cal 1 . B: Quartzite mylonite containing dynamically recrystallized
Qtz 1 with recrystallization at grain boundaries. C: Crenulations cleavage overprinting
mylonitized amphibolite. D: Isoclinal recumbent F1 and F2 folds with a dominant ESE axial
plane foliation, and overprinted by an NNW trending open upright F3 fold producing a type
2 interference structure in amphibolite rock. E: Albite paragneiss containing lenticular mica
fish, Chl 1 and Bt 1 alternating with recrystallized Qtz 1 . F: Cataclasite of the granite gneiss
showing fragmented mylonite rock and broken Qtz 1 and Kfs 1 embedded in a matrix made of
milled Qtz 1 , Src 2 , Hem 3 , Cal 2 and Chl 3 . G: Breccias of granite gneiss with Cal 8 -filled matrix
embedding fragments of cataclasite. H: Breccias with matrix embedding amphibolite
fragments. I: Field photo of the Martin Lake basal conglomerate composed of granite,
quartzite and amphibolite fragments embedded in a hematized matrix. J: Late Cal 11 , Qtz 5
43

and Hem 9 veins cutting the amphibolite. Pen indicates north. Chl: chlorite, Hem: hematite,
Kfs: potassium feldspar, Ms: muscovite, Qtz: quartz, Src: sericite, U: uraninite.
The albite paragneiss occurs in the footwall of the fault. It is mylonitized and
composed of Bt 1 biotite, Chl 1 chlorite, Ms 1 muscovite, and Ab 1 albite. In thin section, the
rocks display a mylonitic fabric with strained Ab 1 albite and Kfs 1 feldspars porphyroclasts
and recrystallized Qtz 1 quartz (Fig. 2.7E). The Ab 1 albite porphyroclasts are wrapped by
Chl 1 chlorite and Src 1 sericite.
The granite gneiss occurs along zones of brecciation and mylonitization in the
footwall (Fig. 2.6B). The rock is fractured and veined and displays a mylonitic fabric with
foliation parallel to the Saint Louis fault. It is generally cataclastic or brecciated. The
cataclasite is composed of broken Qtz 1 quartz and Kfs 1 feldspars clasts, and fragments of
mylonite rocks embedded in a matrix of Qtz 1 quartz, Cal 2 calcite, Src 2 sericite, and Chl 3
chlorite (Fig. 2.7F). The breccia consists of angular mylonite and cataclasite fragments
embedded in a Cal 8 calcite and Chl 7 chlorite-dominated matrix (Fig. 2.7G).
The Martin Lake basal conglomerates uncomformably overlie the granitic gneiss in
the hanging wall of the fault (Fig. 2.6). The conglomerate contains angular fragments of
granite, quartzite and amphibolite embedded in a sandy to silty, medium-grained matrix
(Fig. 2.7H).
The Foot Bay gneiss contains a mylonitic foliation and a NE-trending lineation
defined by a mineral assemblage Hbl 1 +Kfs 1 +Pl 1 +Bt 1 +Qtz 1
consistent with shear
deformation at amphibolite grade metamorphism. Locally, Bt 1 biotite replaces Hbl 1
hornblende. Chl 1 chlorite is common as a retrograde product of Bt 1 biotite. Src 1 sericite
44

eplaces Kfs 1
feldspars (Fig. 2.7A). The overlying Donaldson Lake gneiss has a
metamorphic assemblage Bt 1 +Pl 1 +Src 1 +Chl 1 +Qtz 1 typical of greenschist grade
metamorphism. The Fay Mine Complex is more deformed than the underlying Foot Bay
and Donaldson Lake gneisses with a mineral assemblage Chl 1 +Src 1 +Ab 1 +Qtz 1 consistent
with lower greenschist facies metamorphism. In the cataclasite and breccia rocks, calcite,
chlorite, quartz, hematite and sericite are the dominant alteration minerals (Figs. 2.7F and
2.7G).
Late Chl 9 chlorite, Cal 11 calcite, Qtz 5 quartz, and Hem 9 hematite veins (Fig. 2.7J) and
mafic dikes cut across the Saint Louis fault.
2.4.3. Paragenesis of the alteration and ore minerals and type of U mineralization
The sequence of deformation and alteration is divided into seven events including six
stages of uranium mineralization, based on petrographic, structural, and age relationships
(Figs. 2.8 and 2.9).
2.4.3.1. Stage 1: Mylonitization
Mylonitization is the earliest deformation observed. The quartzo-feldspathic
mylonite at Cinch Lake and the Foot Bay gneiss at Ace-Fay exhibit recrystallized Qtz 1
quartz around rotated Kfs 1 feldspars. The hornblende-feldspar gneiss at Cinch Lake and the
Foot Bay gneiss at Ace-Fay define an amphibolite metamorphic assemblage
Kfs 1 +Pl 1 +Hbl 1 (Fig. 2.4D). Retrogression to greenschist metamorphic grade is indicated by
the assemblage Bt 1 +Chl 1 +Src 1 +Hem 1 +Qtz 1 . Early Py 1 pyrite, Cpy 1 chalcopyrite and Nl 1
nolanite are stretched along the foliation (Fig. 2.8).
45

Figure 2.8. Generalized paragenesis of the uranium mineralization, metamorphic
relationships and deformation sequences in the Beaverlodge area. The paragenesis is based on
petrographic, metamorphic and structural observations, style of uranium mineralization and
associated deformation, and geochronology data of various paragenetically constrained
uranium grains. Note: The thickness of the horizontal line is proportional to the abundance of
the mineral. The main uranium mineralization event is associated with the brecciation stage.
The mylonitic foliation is cut by Chl 2 chlorite, Qtz 2 quartz, Ab 1 albite, Cal 1 calcite,
and Ep 1 epidote veinlets (Fig. 2.8).
2.4.3.2. Stage 2: Cataclasite deformation:
Cataclasite resulted from a ductile-brittle reactivation of the mylonite. The cataclasite
rocks are composed of Qtz 1 quartz and Kfs 1 feldspars clasts, and crushed Cal 1 calcite and
Qtz 2
quartz veinlets embedded in a matrix composed of disseminated ±U 1 uraninite
associated with Cal 2 calcite, Hem 3 hematite, Chl 3 chlorite, Src 2 sericite, Cpy 2 chalcopyrite,
and Py 2 pyrite (Figs. 2.8 and 2.9A).
2.4.3.3. Stage 3: Early tensional ±U 2 veins formation
Cataclasite rocks are cut by early tensional Qtz 3 +Cal 3 -±U 2 veins. U 2 uraninite is
associated with Cal 4 calcite, Chl 4 chlorite, Hem 4 hematite, and Py 3 pyrite (Fig. 2.9B). Qtz 3
quartz and Cal 3 calcite veins display evidence of tensional fractures that contain syntaxial
fibers growth perpendicular to the wall of the vein (Fig. 2.9B). Syntaxial Cal 3 calcite vein
fill the core of the Qtz 3 quartz vein.
2.4.3.4. Stage 4: Granite-related metasomatic alteration in the Gunnar deposit
Ab 2 albite alteration of the Gunnar granite is pervasive and results in the
“dequartzification” of the granite. Replacement of Kfs 1 feldspars is complete and precedes
47

the Qtz 1 quartz dissolution resulting in a rock composed of Ab 2 albite (Fig. 2.9C), which is
further Cal 5 carbonatized. Cal 5 calcite occupies voids left after Qtz 1 quartz dissolution. The
U 3 mineralization is introduced during late stage albitization and occupies space between
Ab 2 albite grains likely derived from Cal 5 calcite and Qtz 1 quartz dissolution. U 3 uraninite
is associated with Chl 5 chlorite, Src 3 sericite, Hem 5 hematite, Cal 6 calcite, Mnz 1 monazite
and Ttn 2 titanite (Figs. 2.8 and 2.9C). Late alteration associated with Cal 7 calcite, Qtz 4
quartz and Chl 6 chlorite veins cut the albitized and U 3 -mineralized granite.
2.4.3.5. Stage 5: Brecciation
The breccia is composed of angular fragments of cataclasite and mylonite rocks
embedded in a Cal 8 calcite-rich matrix. The matrix also contains broken Qtz 1 quartz and
Kfs 1 feldspar fragments of variable size (0.1 to 2 mm). U 4 uraninite typically surrounds
hematized fragments and occurs as grains disseminated into the matrix (Fig. 2.9D).
Locally, massive U 4 uraninite associated with minor Cal 8 calcite makes up the bulk of the
matrix. U 4 uraninite is commonly associated with brannerite Br 1 , Chl 7 chlorite, Src 3
sericite, Hem 6 hematite, Py 5 pyrite, and Cpy 4 chalcopyrite and is the major uranium
mineralizing event (Figs. 2.8 and 2.9D).
2.4.3.6. Stage 6: Mafic volcanism
U mineralization associated with mafic dikes is in the form of massive ±U 5 uraninite
veins and as grains disseminated into breccia-dikes (Figs. 5K and 9E) that cut across the
shear zone at the Cinch Lake deposit. U 5 uraninite is associated with Cal 9 calcite, Chl 8
chlorite, Hem 7 hematite, Ap 1 apatite, Src 4 sericite, Ttn 3 titanite, Mnz 2 monazite, Py 6 pyrite,
and Cpy 5 chalcopyrite (Fig. 2.8).
48

2.4.3.7. Stage 7: Late U 6 uraninite veins
U 6 uraninite veins (Fig. 2.9F) cut all previous rocks and are the youngest observed
mineralized phase. These veins cut the Martin Lake basal conglomerates and the mafic
dikes and contain ±U 6 uraninite, Cal 10 calcite, Chl 9 chlorite, Hem 8 hematite and Py 7 pyrite
(Fig. 2.8).
49

Figure 2.9. Microphotograph of typical mineral assemblages and crosscutting relationships
from the Ace-Fay-Verna, Cinch Lake and Gunnar uranium deposits: A: Cataclasite with
mylonitized fragments, Qtz 1 , Kfs 1 in a matrix composed of ±U 1 , Qtz 1 , Cal 2 , Hem 3 , Chl 3 , Src 2 ,
Cpy 2 and Py 2 (Sample 6122-Cat, Ace deposit). B: U 2 -Hem 4 -Cl 4 -Cal 4 -Py 3 vein cutting
cataclasite rock and filled by tensional vein of Qtz 3 and Cal 3 (Sample 6122BV-Cat, Ace
deposit). C: Mineralized metasomatic granite in Gunnar: U 3 fills voids felt after Qtz 1
dissolution and is associated with Chl 5 , Src 3 , Hem 5 , Mnz 1 , Cal 5 and Ttn 2 (Sample GN-05,
Gunnar). D: Breccia with fragments of cataclasite rock in a Cal 8 -rich matrix. U 4 surrounds
breccia fragments and is disseminated in matrix associated with Chl 7 , Src 3 , and Hem 6 (Sample
B5812, Ace-Fay deposit). E: Mafic volcanic-type ±U 5 : hydro-breccia vein composed of crushed
Qtz 1 and Kfs 1 fragments and Cal 9 embedded in a Chl 8 -rich matrix. U 5 is associated with Hem 7 ,
Ap 1 , Src 4 , Ttn 3 , Mnz 2 , Py 6 , and Cpy 5 (Sample Cl-45, Cinch Lake deposit). F: Late mineralized
veins containing U 6 , Cal 10 , Chl 9 , Hem 8 . G: Late Cal 11 , Chl 10 and Qtz 5 veins (Sample 2202,
Martin Lake deposit). H: Late sulphide minerals composed of Gn 1 , Cpy 5 and Py 8 and Sp 1
(Sample B5800, Ace-Fay deposit). Ap: apatite, Cal: calcite, Chl: chlorite, Cpy: chalcopyrite,
50

Hem: hematite, Kfs: potassium feldspar, Ms: muscovite, Mnz: monazite, Py: pyrite, Qtz:
quartz, Src: sericite, Ttn: titanite, U: uraninite.
2.4.4. Geochronology of uraninite and isotopic systematics
The various generations of uraninite that formed during different stages of
deformation have been paragenetically constrained (see previous section), and analyzed.
For example the cataclasite-type ±U 1 and early-vein type ±U 2 uraninites observed at the
Ace-Fay deposits formed at depth different from the breccia-type U 4
uraninite. The
granite-related metasomatic-type U 3 uraninite is observed at Gunnar wherein moderate
uranium mineralization is derived from Na-metasomatism of the Gunnar granite prior to
brecciation. The volcanic-type ±U 5 uraninite cuts across the ductile-brittle shear zones at
Cinch Lake and Ace-Fay deposits and is spatially related to the Martin Lake mafic dikes.
Late ±U 6 uraninite veins interpreted as related to the Athabasca Basin, cross cut all types
and have a distinct alteration assemblage.
2.4.4.1. U-Pb and Pb-Pb geochronology of U-rich minerals by LA-HR-ICP-MS
Paragenetically constrained uraninite grains from the six stages of uranium
mineralization have been dated by LA-HR-ICP-MS (Table 2.1). Results of the U-Pb
concordia are summarized in Table 2.2a. The oldest 207 Pb/ 206 Pb ages are likely to be closer
to the initial formation age because Pb/Pb ratios in uraninite are less susceptible to
resetting by younger fluid events than are the U/Pb ratios (Collins et al., 1954). The
relatively high error margins for U/Pb isotopic ratios reflect uraninite heterogeneity
(Kotzer and Kyser, 1993; Chipley et al., 2007), which is indicated by the mottled and
pitted texture observed in Back-Scattered Electron Microscopy (BSEM) images of
51

uraninite (Fig. 2.10). The errors observed in the U-Pb systems are in large part a function
of the uraninite age; older uraninite is more likely to have been affected by multiple
alteration events so that errors obtained in the U-Pb system are greater. The youngest
uraninites, which are recrystallized forms of older uraninites, have the lowest error and are
least altered.
52

Sample I.D Mineralization-type Deposit n
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
Oldest
207 Pb/ 206 Pb
±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
a. Primary uranium mineralization
Cat Cataclasite-type U 1 Ace Fay 15 0.1170 0.0024 3.7511 0.6756 0.2442 0.0655 0.54 1896 37 2272 27 1403 340 1572 147 25
6122a Cataclasite-type U 1 Ace Fay 11 0.1241 0.0018 3.9547 0.3658 0.2477 0.0273 0.56 2002 26 2293 17 1425 373 1615 111 28
6122b Early vein-type U 2 Ace Fay 16 0.1041 0.0020 3.3142 0.4428 0.2452 0.0529 0.50 1674 36 2289 20 1409 272 1470 103 14
V-Cat Early vein-type U 2 Ace Fay 11 0.1189 0.0021 3.6762 0.5656 0.2563 0.0629 0.52 1915 34 2276 29 1469 323 1562 123 21
B5812a Breccia-type U 4 Ace Fay 8 0.1098 0.0026 2.7659 0.1271 0.1710 0.0133 0.44 1796 43 1848 5 1016 74 1339 31 43
6120 Volcanic-type U 5 Ace Fay 12 0.1076 0.0005 3.4210 0.1909 0.2314 0.0136 0.95 1760 9 1800 37 1340 71 1505 44 24
6139 Volcanic-type U 5 Gunnar 22 0.1096 0.0003 4.1894 0.307 0.2795 0.0207 1.00 1793 4 1812 15 1587 104 1669 61 11
2202 Athabasca-type U 6 Martin Lake 37 0.0897 0.0004 2.1196 0.138 0.1717 0.0111 1.00 1418 9 1620 4 1020 61 1147 44 28
3705 Athabasca-type U 6 Ace Fay 22 0.0914 0.0090 2.2412 0.391 0.1924 0.0412 0.63 1453 188 1616 174 1125 220 1158 123 24
b. Post-mineralization alteration events recorded in the U/Pb system
VRC Breccia-type U 4 Gunnar 14 0.0857 0.0004 1.6237 0.0676 0.1374 0.0057 0.99 1331 10 1380 34 828 32 973 26 38
6134 Metasomatic-type U 3 Gunnar 7 0.0832 0.0019 0.2582 0.0268 0.0224 0.0024 0.74 1268 48 1372 4 142 15 227 20 89
GN-42 Metasomatic-type U 3 Gunnar 11 0.0806 0.0011 0.3779 0.0275 0.0340 0.0025 0.98 1210 26 1284 22 215 15 325 20 82
C23-116 Breccia-type U 4 Cinch Lake 29 0.0705 0.0014 0.4164 0.0526 0.0427 0.0055 0.96 930 41 1164 24 268 34 340 38 69
VR69190 Metasomatic-type U 3 Gunnar 10 0.0653 0.0006 0.6351 0.0451 0.0705 0.0050 0.99 786 19 796 15 439 30 499 28 44
6037b Metasomatic-type U 3 Gunnar 10 0.0536 0.0014 0.2358 0.0473 0.0318 0.0059 0.977 352 61 497 26 201 36 213 37 43
EA3010A Athabasca-type U 6 Eagle-Ace 10 0.0534 0.0003 0.2626 0.0198 0.0356 0.0027 1.00 347 14 396 13 225 17 237 16 35
EA3011 Volcanic-type U 5 Eagle-Ace 15 0.0529 0.0006 0.2389 0.0170 0.0327 0.0023 0.98 325 28 419 21 207 14 217 14 36
Table 2.1. Analytical data from the U/Pb LA-HR-ICP-MS analysis of various uraninite occurrences in the Beaverlodge area. The
paragenesis of each type of uraninite analyzed is shown in Figures 2.8 and 2.9 and described in Section 4.3., R: error correlation
coefficient, Disc‡: percentage discordance. n: number of grains. 206 Pb/ 238 U, 207 Pb/ 235 U, and 207 Pb/ 206 Pb ages are calculated using equations
reported by Ludwig (2000) and expressed in Ma.
53

Figure 2.10. Backscattered Electron Microscope (BSEM) of U-rich minerals. A: Mottled and
speckled U 1 grain disseminated in cataclasite rock (Sample 6122, Ace). B: Speckled and pitted
U 2 grain in early tensional vein showing ablation pits created by LA-HR-ICPMS (Sample
6122, Ace). C: Fractured and altered U 3 (Sample 6134, Gunnar). D: Recrystallized U 3 coating
vugs in altered metasomatic granite (Sample 6134, Gunnar). E: Speckled and pitted U 4
54

(Sample 6137, Gunnar). F: Pitted, mottled and heterogeneous U 4 from breccia-type (Sample
B5812, Fay).
Uraninite -type
Deposit
a. Primary uranium mineralization.
Upper
intercept age
(Ma)
Lower
intercept
age (Ma)
207 Pb/ 206 Pb
age (Ma)
MSWD
Figure
Cataclasite-type U 1 Fay 2306±360 907±330 2293±17 0.13 11A
Early vein-type U 2 Fay 1594±95 89±670 2289±20 0.089 11B
Breccia-type U 4 Ace-Fay 1857±170 42±350 1848±5 0.5 11C
Volcanic-type U 5 Ace-Fay 1783±7 71±79 1812±15 6.2 11D
Volcanic-type U 5 Gunnar 1774±25 109±110 1800±37 1.14 11E
Athabasca-type U 6 Martin Lake 1601±64 441±92 1620±4 10 11F
b. Post-mineralization alteration events recorded in altered uraninite
Metasomatic-type U 3 Gunnar 1549±78 75±13 1210±25 1.02 11G
Breccia-type U 4 Fay 1355±40 54±87 1330±10 0.59 11H
Metasomatic-type U 3 Gunnar 1219±230 13±53 352±31 3.5 11I
Breccia-type U 4 Cinch Lake 1094±66 28±31 1019±44 0.57 11J
Metasomatic-type U 3 Gunnar 818±47 47±61 786±19 0.13 11K
Athabasca-type U 6 Eagle 635±170 166±30 347±14 0.42 11L
Volcanic-type U 5 Eagle-Ace 439±56 103±29 325±28 1.4 11M
Metasomatic-type U 3 Gunnar 391±40 31±150 352±61 0.18 11N
Table 2.2. Summary of the U-Pb concordia results of U-rich minerals for various events of: a)
primary uranium mineralization and b) post-mineralization alteration and resetting events in
the Beaverlodge area. Figure refers to figure in text that shows the mode of occurrence of the
uraninite.
2.4.4.1.1. Geochronology of the cataclasite-type ±U 1
U 1 uraninite has U-Pb isotopic compositions that define a discordia line and groups
of 207 Pb/ 206 Pb ages (Fig. 2.11A, Table 2.1). The discordia line has an upper intercept age of
2306±360 Ma and a lower intercept of 907±330 Ma (2σ, MSWD: 0.13). The oldest
207 Pb/ 206 Pb age is 2293±17 Ma, which overlaps the upper intercept age and is interpreted as
the minimum formation age. The 207 Pb/ 206 Pb system displays five groups of age that reflect
55

post-mineralization alteration during the intervals of 2.2-2.1 Ga, 2.1-2.0 Ga, 2.0-1.9 Ga,
1.9-1.8 Ga, and 1.6 Ga (Table 2.1 and Appendix 1).
2.4.4.1.2. Geochronology of the early tensional vein-type ±U 2
U 2 uraninite gives a discordant U-Pb upper-intercept age of 1594±95 Ma and a lower
intercept of 89±670 Ma (Fig. 2.11B). The oldest 207 Pb/ 206 Pb age of 2289±20 Ma is
interpreted as a minimum crystallization age. The 207 Pb/ 206 Pb system shows alteration
events at ca. 2.2-2.1 Ga, 2.1-2.0 Ga, 2.0-1.9 Ga, 1.9-1.8 Ga, and 1.6 Ga (Table 2.1, Fig.
2.11, and Appendix 1).
2.4.4.1.3. Geochronology of the granite-related metasomatic-type U 3 in Gunnar
U/Pb isotopic ratios of U 3 are discordant with very low Pb/U ratios that indicate
significant Pb loss. Ages obtained in the U/Pb system range between 1550 to 10 Ma
(Tables 2.1b and 2.2b) and do not reflect the formation age of the granite-related
metasomatic-type U mineralization because of substantial Pb loss. Rather they reflect
periods of alteration that have significantly affected U 3 subsequent to its formation.
2.4.4.1.4. Geochronology of the breccia-type U 4
U/Pb isotopic ratios of U 4 , which reflect the major uranium mineralizing event, are
discordant and yield a U-Pb upper-intercept age of 1857±170 Ma (2σ, MSWD: 0.5) and a
lower intercept of 42±350 (Fig. 2.11C). The oldest 207 Pb/ 206 Pb age of 1848±5 Ma records
the minimum crystallization age. Post-mineralization alteration recorded in the 207 Pb/ 206 Pb
ratios occur at ca. 1.8 Ga, 1.4-1.3 Ga, 1.2-0.9 Ga, 0.8 Ga and 0.5 Ga (Table 2.1).
2.4.4.1.5. Geochronology of the volcanic-type ±U 5
56

U 5 uraninite yields two discordia lines. The concordia in Figure 2.11D has an upper
intercept age of 1783±7 Ma and a lower intercept of 71±79 Ma, with an oldest 207 Pb/ 206 Pb
age of 1812±15 Ma (2σ, MSWD: 6.2). The concordia in Figure 2.11E has an upper
intercept age of 1774±25 Ma and a lower intercept of 109±110 Ma (2σ, MSWD: 1.14).
The oldest 207 Pb/ 206 Pb age is 1800±37 Ma. The 207 Pb/ 206 Pb system records periods of
alteration at ca. 0.8-0.7 Ga and 0.4-0.3 Ga (Table 2.1).
2.4.4.1.6. Geochronology of the Athabasca-related ±U 6 :
U 6 uraninite gives a U-Pb concordia upper-intercept age of 1601±64 Ma and a lower
intercept of 441±92 Ma (2σ, MSWD: 10) (Fig. 2.11F). The oldest 207 Pb/ 206 Pb age of
1620±4 Ma is interpreted as the formation age. Post-mineralization alterations recorded in
the 207 Pb/ 206 Pb system occur at ca. 1.4-1.3 Ga and 0.4-0.3 Ga (Table 2.1).
2.4.4.1.7. Post-mineralization alteration events recorded in the U/Pb system
The U/Pb system records various episodes of post-mineralization alteration that have
affected all stages of the uranium mineralization. Results are presented in Figures 2.11G to
2.11N and summarized in Table 2.2b.
U/Pb age of the primary uranium mineralization
57

Post-mineralization alteration events recorded in the U/Pb system
58

Figure 2.11. U-Pb concordia diagrams from in situ isotopic analysis by LA-HR-ICP-MS of U
from various deposits in the Beaverlodge area. A: Cataclasite-type ±U 1 (Sample 6122-Cat, Ace
deposit). B: Early tensional vein-type ±U 2 (Sample 6122BV-Cat, Ace deposit). C: Breccia-type
U 4 (Sample B5812, Ace-Fay deposit). D: Volcanic-type ±U 5 (Sample 6120, Ace-Fay deposit). E:
59

Volcanic-type ±U 5 (Sample 6139, Gunnar deposit). F: Athabasca-related ±U 6 (Sample 2202,
Martin Lake deposit). G: Altered metasomatic-type U 3 (Sample GN-42, Gunnar deposit). H:
Altered breccia-type U 4 at Gunnar (Sample VR, Gunnar deposit). I: Altered breccia-type U 4
(Sample C23-116, Cinch Lake deposit). J: Altered metasomatic-type U 3 (Sample 6134,
Gunnar deposit). K: Altered Athabasca-related ±U 6 (Sample EA3011, Eagle-Ace). L: Altered
volcanic-type ±U 5 (Sample AE3010, Eagle-Ace deposit). M: Altered metasomatic-type U 3
(Sample VR69190, Gunnar deposit). Note: Data-point error ellipses are 2σ. Plots were
constructed using ISOPLOT ver. 3.2 (Ludwig 2000) from the isotope ratios and their
respective errors are presented in Table 2.1. 207 Pb/ 206 Pb ages are reported along discordia line,
the oldest 207 Pb/ 206 Pb age is shown in bold character for concordia of the primary U
mineralization.
2.4.4.2. Chemical Pb age of the uranium mineralization
Regression of the sum SiO 2 , Fe 2 O 3 , CaO and MnO contents to zero in the early veintype
±U 2
uraninite corresponds to 2290 Ma (Fig. 2.12A), which is identical to the
207 Pb/ 206 Pb formation age of 2293±17 Ma (Fig. 2.11B). Chemical Pb ages show alteration
events at ca. 1800 Ma, 1600 Ma, 1200 Ma, and 170 Ma (Table 2.3).
Chemical Pb ages derived from the composition of the breccia-type U 4 uraninite vary
from 1315 Ma to 557 Ma. The intercept at zero content of elements other than uraninite
gives an age of 1830 Ma (Fig. 2.12B), which is close to the 207 Pb/ 206 Pb formation age of
1848±5 Ma (Fig. 2.11D).
The zero intercept of the Chemical Pb age of the volcanic-type ±U 5
uraninite
corresponds to 1827 Ma (Fig. 2.12C), which overlaps the 207 Pb/ 206 Pb ages of 1812±15 Ma
and 1800±37 Ma (Figs. 11D and 11E, respectively). The concordance of these ages is
interpreted as the crystallization age of ±U 5 uraninite. Chemical Pb ages display alteration
events at ca. 1800-1700 Ma, 1500-1400 Ma, and 1300-1200 Ma (Table 2.3).
60

Sample I.D Deposit UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Chemical
Pb age
(Ma)
Early vein-type U 2 uraninite
6122_Pt2 1 Ace Fay 71.83 2.02 3.61 0.39 0.40 0.03 0.11 17.88 0.02 0.03 0.02 0.05 0.12 0.00 0.14 0.03 96.50 1544
6122_Pt3 1 Ace Fay 73.07 3.05 3.45 0.91 0.38 0.05 0.03 14.52 0.04 0.10 0.02 0.02 0.15 0.07 0.11 0.07 95.90 1233
6122_Pt4_2 Ace Fay 72.61 0.59 3.33 0.31 0.65 0.02 0.04 17.42 0.03 0.02 0.02 0.03 0.18 0.04 0.02 0.00 95.29 1488
6122_Pt5_1 Ace Fay 71.65 0.46 2.32 0.11 0.38 0.04 0.06 19.91 0.02 0.05 0.01 0.01 0.07 0.09 0.01 0.02 95.10 1724
6122_Pt10 1 Ace Fay 73.64 9.89 2.48 1.14 1.36 0.28 0.23 1.90 0.36 0.06 0.01 0.03 0.36 0.08 0.20 0.05 91.80 160
Metasomatic-type U 3 uraninite
6134 pt2 1 Gunnar 77.59 3.01 5.35 0.15 0.06 0.01 0.04 0.07 0.12 0.14 0.01 0.01 0.03 0.02 0.07 0.04 86.61 5
6134 pt2 2 Gunnar 80.25 3.04 5.60 0.23 0.03 0.01 0.09 0.12 0.00 0.08 0.03 0.00 0.08 0.04 0.06 0.04 89.46 9
6134 pt2 3 Gunnar 78.63 3.65 5.19 1.65 0.33 0.01 0.06 0.00 0.06 0.07 0.02 0.02 0.06 0.00 0.07 0.12 89.78 0
6134 pt2 4 Gunnar 78.36 3.72 5.28 1.82 0.44 0.05 0.02 0.03 0.06 0.06 0.05 0.02 0.06 0.01 0.05 0.02 89.85 2
6134 pt3 Gunnar 77.88 4.95 5.57 0.19 0.37 0.01 0.01 0.12 0.05 0.07 0.03 0.01 0.09 0.01 0.08 0.01 89.33 9
6134 pt3 1 Gunnar 79.27 3.95 5.52 0.15 0.01 0.03 0.04 0.11 0.08 0.08 0.04 0.01 0.03 0.00 0.04 0.02 89.22 9
6134 pt3 2 Gunnar 81.64 3.39 4.56 0.16 0.00 0.12 0.07 0.03 0.05 0.06 0.04 0.00 0.07 0.03 0.08 0.05 90.13 2
6134 pt3 3 Gunnar 79.50 3.78 5.54 0.11 0.06 0.04 0.02 0.06 0.09 0.06 0.02 0.00 0.04 0.00 0.06 0.01 89.23 4
6134 pt4 1 Gunnar 80.77 3.52 5.67 0.23 0.01 0.01 0.00 0.13 0.01 0.07 0.03 0.01 0.09 0.04 0.01 0.04 90.58 10
6134 pt4 2 Gunnar 79.52 3.13 5.90 0.26 0.13 0.01 0.03 0.09 0.07 0.05 0.00 0.03 0.07 0.01 0.03 0.01 89.31 7
6134 pt4 3 Gunnar 81.29 2.79 5.67 0.20 0.03 0.00 0.02 0.16 0.01 0.05 0.02 0.00 0.07 0.03 0.04 0.02 90.29 12
6134 pt5 1 Gunnar 81.39 2.70 5.41 0.13 0.00 0.04 0.00 0.11 0.04 0.06 0.07 0.00 0.05 0.06 0.02 0.07 89.88 8
6134 pt5 2 Gunnar 74.27 3.20 4.97 0.22 0.08 0.04 0.02 0.04 0.11 0.23 0.02 0.01 0.10 0.02 0.05 0.04 83.27 3
6134 pt5 3 Gunnar 80.12 4.95 4.54 0.22 0.41 0.01 0.01 0.10 0.12 0.12 0.05 0.01 0.02 0.16 0.01 0.01 90.75 8
6134 pt6 1 Gunnar 81.12 3.04 5.23 0.01 0.01 0.04 0.01 0.03 0.00 0.04 0.02 0.01 0.01 0.01 0.02 0.01 89.49 2
6134 pt6 2 Gunnar 81.92 3.06 5.25 0.04 0.04 0.00 0.00 0.10 0.01 0.04 0.02 0.00 0.08 0.04 0.04 0.04 90.45 7
6134 pt6 3 Gunnar 80.49 3.09 5.36 0.02 0.02 0.01 0.09 0.08 0.04 0.06 0.01 0.01 0.01 0.04 0.09 0.01 89.37 6
6134 pt6 4 Gunnar 81.96 3.12 4.98 0.05 0.04 0.01 0.02 0.10 0.02 0.06 0.04 0.00 0.07 0.02 0.01 0.01 90.44 8
6134 pt8 1 Gunnar 79.17 2.87 4.43 0.01 0.02 0.01 0.57 1.40 0.09 0.07 0.02 0.10 0.03 0.16 0.07 0.01 88.96 110
6134 pt8 2 Gunnar 79.67 2.90 4.69 0.02 0.07 0.03 0.35 1.44 0.06 0.00 0.03 0.07 0.02 0.08 0.10 0.05 89.42 112
6134 pt8 3 Gunnar 80.29 3.14 3.87 0.03 0.78 0.01 0.05 0.11 0.08 0.03 0.04 0.00 0.04 0.12 0.00 0.00 88.53 9
6134 pt8 4 Gunnar 77.08 2.76 5.44 0.05 0.02 0.02 0.53 0.61 0.09 0.01 0.01 0.04 0.06 0.21 0.02 0.04 86.86 49
6134 pt8a 1 Gunnar 80.50 4.02 5.50 0.04 0.11 0.02 0.00 0.07 0.01 0.12 0.06 0.02 0.07 0.05 0.03 0.00 90.45 5
61

6134 pt8a 2 Gunnar 82.92 2.92 5.30 0.07 0.04 0.02 0.09 0.11 0.01 0.07 0.01 0.04 0.10 0.01 0.07 0.02 91.62 8
6134 pt8a 3 Gunnar 77.51 1.83 5.81 0.17 0.02 0.02 0.05 0.16 0.11 0.15 0.00 0.03 0.12 0.01 0.06 0.07 85.99 13
6134 pt9 1 Gunnar 63.41 3.15 4.32 0.08 0.04 0.03 0.24 1.46 0.18 0.19 0.03 0.05 0.08 0.12 0.05 0.02 73.42 143
6134 pt9 2 Gunnar 75.28 3.78 5.33 0.02 0.07 0.01 0.29 1.41 0.22 0.08 0.00 0.03 0.01 0.20 0.02 0.07 86.69 117
6134 pt9 3 Gunnar 73.41 2.98 5.19 0.09 0.09 0.05 0.31 1.60 0.28 0.29 0.03 0.02 0.07 0.19 0.06 0.03 84.62 135
6134 pt9a 1 Gunnar 81.55 3.36 4.26 0.18 0.69 0.00 0.08 0.08 0.15 0.10 0.01 0.01 0.06 0.07 0.02 0.00 90.57 6
6134 pt9a 2 Gunnar 80.44 2.93 4.23 0.04 0.47 0.06 0.14 0.21 0.15 0.07 0.01 0.01 0.05 0.13 0.02 0.04 88.96 16
6134 pt9a 3 Gunnar 78.82 3.02 4.69 0.03 0.60 0.03 0.15 0.05 0.14 0.05 0.01 0.00 0.03 0.15 0.04 0.05 87.79 4
6134 pt9a 4 Gunnar 77.24 5.45 4.77 0.44 0.46 0.04 0.00 0.12 0.19 0.16 0.00 0.01 0.09 0.16 0.05 0.03 89.07 10
6134 pt10 1 Gunnar 73.83 6.55 3.47 1.32 0.01 0.03 0.07 0.41 0.09 0.14 0.00 0.01 0.05 0.27 0.01 0.06 86.09 35
6134 pt10 2 Gunnar 64.50 9.49 2.43 9.15 0.06 0.01 0.12 0.65 0.12 0.28 0.06 0.03 0.05 0.32 0.26 0.05 87.17 63
6134 pt10 3 Gunnar 74.14 7.47 3.23 1.59 0.01 0.01 0.06 0.32 0.04 0.16 0.00 0.01 0.01 0.27 0.03 0.04 87.34 27
6134 pt10 4 Gunnar 74.03 5.88 2.71 1.97 0.08 0.01 0.18 1.96 0.14 0.13 0.03 0.01 0.01 0.41 0.03 0.07 87.58 164
6134 pt10 5 Gunnar 72.59 6.19 3.29 2.40 0.04 0.02 0.08 1.39 0.14 0.15 0.02 0.01 0.03 0.26 0.11 0.01 86.58 119
Breccia-type U 4 uraninite
5812 Pt1 1 Gunnar 75.59 0.50 4.51 0.62 0.46 0.03 0.18 12.07 0.02 0.04 0.03 0.01 0.42 0.45 0.08 0.05 94.92 991
5812 Pt6 2 Ace Fay 34.12 48.31 1.48 1.21 0.18 0.02 0.01 3.86 0.65 0.08 0.03 0.59 0.24 0.14 0.09 0.05 90.96 702
5812 Pt6 1 Ace Fay 74.88 0.54 4.43 0.44 0.44 0.01 0.16 15.88 0.02 0.03 0.02 0.01 0.22 0.15 0.04 0.00 97.16 1315
5812 Pt1 2 Ace Fay 76.71 0.98 6.43 0.90 0.61 0.03 0.21 6.89 0.01 0.03 0.04 0.06 0.70 0.60 0.00 0.01 94.18 557
5812 Pt8 1 Ace Fay 77.99 1.05 4.27 1.20 0.80 0.05 0.01 8.71 0.02 0.03 0.29 0.03 0.35 0.06 0.05 0.02 94.82 693
5812 Pt2 2 Ace Fay 75.02 2.40 4.63 1.28 1.74 0.01 0.14 10.07 0.05 0.06 0.03 0.73 0.67 0.31 0.11 0.03 97.15 832
Volcanic-type U 5 uraninite
6120B_pt4 2 Ace Fay 74.34 1.13 4.30 0.95 0.43 0.02 0.26 14.17 0.05 0.03 0.01 0.01 0.23 0.04 0.02 0.00 95.92 1183
6120B_pt3 1 Ace Fay 74.41 0.84 3.66 0.48 0.65 0.01 0.22 15.41 0.06 0.03 0.02 0.02 0.20 0.03 0.09 0.03 95.99 1285
6120B_pt3 2 Ace Fay 74.38 1.68 2.57 0.54 0.58 0.03 0.13 15.68 0.03 0.03 0.00 0.02 0.10 0.09 0.00 0.03 95.82 1307
6120B_pt2 2 Ace Fay 71.88 1.43 3.00 0.46 0.48 0.03 0.25 17.14 0.06 0.02 0.00 0.01 0.08 0.01 0.07 0.03 94.86 1479
6120B_pt1 2 Ace Fay 73.42 1.05 2.73 0.45 0.52 0.01 0.48 17.56 0.06 0.03 0.07 0.04 0.12 0.01 0.04 0.07 96.46 1484
6120B_pt3 3 Ace Fay 73.75 0.47 3.05 0.29 0.42 0.03 0.09 17.91 0.05 0.04 0.05 0.00 0.07 0.03 0.06 0.04 96.19 1506
6120B_pt5 2 Ace Fay 73.23 0.46 2.58 0.43 0.37 0.03 0.04 19.04 0.03 0.03 0.01 0.01 0.07 0.06 0.03 0.03 96.37 1613
6120B_pt6 1 Ace Fay 71.73 0.92 2.35 0.28 0.49 0.04 0.46 19.29 0.04 0.03 0.02 0.03 0.01 0.03 0.05 0.01 95.67 1668
6120B_pt3 4 Ace Fay 74.04 0.50 2.50 0.32 0.30 0.03 0.13 20.15 0.04 0.04 0.02 0.03 0.01 0.02 0.03 0.04 98.05 1689
6120B_pt5 1 Ace Fay 72.87 0.38 2.37 0.23 0.29 0.01 0.16 19.91 0.05 0.02 0.01 0.04 0.04 0.11 0.09 0.03 96.56 1695
62

6120B_pt4 1 Ace Fay 70.14 0.67 2.65 0.15 0.37 0.01 0.33 19.62 0.04 0.02 0.05 0.02 0.08 0.04 0.08 0.01 94.13 1735
6120B_pt4 1 Ace Fay 71.92 0.51 2.33 0.05 0.51 0.01 0.11 20.29 0.03 0.02 0.08 0.04 0.05 0.09 0.06 0.02 95.99 1750
Athabasca-type U 6 uraninite
3705 Pt4 5 Ace Fay 24.22 2.29 0.49 3.46 59.66 0.03 1.23 4.43 0.04 0.02 0.01 0.44 0.01 0.04 0.16 0.00 96.29 1135
3705 Pt3 2 Ace Fay 38.66 4.78 1.74 3.34 36.72 0.06 0.86 5.48 0.01 0.02 0.10 0.40 0.04 0.01 0.22 0.02 92.19 880
3705 Pt3 4 Ace Fay 39.64 6.95 1.09 4.31 36.08 0.04 0.62 3.14 0.30 0.04 0.07 0.00 0.02 0.02 0.07 0.06 92.29 492
3705 Pt4 2 Ace Fay 29.41 9.42 1.69 4.03 36.11 0.08 0.38 1.68 2.70 0.11 0.05 0.01 0.03 0.20 0.11 0.04 85.79 354
3705 Pt4 1 Ace Fay 48.08 10.87 2.67 3.29 16.60 0.00 0.33 5.69 0.84 0.13 0.15 0.86 0.04 0.44 0.20 0.07 89.96 735
3705 Pt4 3 Ace Fay 28.39 8.87 2.09 6.23 44.41 0.02 0.62 2.17 0.18 0.10 0.02 0.01 0.04 0.03 0.26 0.00 93.18 473
3705 Pt2 7 Ace Fay 36.89 10.39 1.29 6.22 33.91 0.01 0.45 0.58 0.74 0.10 0.14 0.01 0.00 0.09 0.18 0.00 90.80 98
3705 Pt2 4 Ace Fay 34.12 11.57 1.16 5.91 33.49 0.01 0.32 0.71 0.77 0.11 0.10 0.01 0.01 0.06 0.10 0.04 88.37 130
3705 Pt4 7 Ace Fay 34.71 11.31 1.27 6.26 34.74 0.01 0.53 0.84 0.64 0.14 0.08 0.02 0.02 0.01 0.13 0.08 90.57 149
3705 Pt2 5 Ace Fay 35.07 11.45 1.29 6.67 36.99 0.01 0.57 0.76 0.61 0.08 0.04 0.00 0.06 0.04 0.15 0.02 93.68 135
3705 Pt4 6 Ace Fay 29.87 12.08 1.98 6.51 36.63 0.22 0.46 1.09 0.58 0.09 0.21 0.00 0.04 0.02 0.20 0.03 89.80 227
3705 Pt4 4 Ace Fay 41.88 16.19 0.63 3.07 28.28 0.01 0.97 0.78 0.30 0.01 0.14 0.00 0.02 0.08 0.12 0.05 92.38 116
3705 Pt2 6 Ace Fay 33.11 13.43 1.46 5.84 36.83 0.02 0.21 1.19 0.62 0.10 0.12 0.02 0.05 0.01 0.20 0.02 93.00 223
3705 Pt2 3 Ace Fay 39.04 16.30 0.64 3.39 28.73 0.07 1.15 0.74 0.30 0.02 0.04 0.01 0.02 0.06 0.10 0.03 90.50 117
3705 Pt3 1 Ace Fay 45.91 17.68 2.01 2.59 16.32 0.01 0.23 0.74 0.95 0.01 0.15 0.00 0.03 0.20 0.09 0.01 86.83 100
Table 2.3. Average chemical composition and calculated chemical Pb ages from electron microprobe analyses of different uraninite
occurrences in the Beaverlodge area. The composition is reported in weight percent and the age in Ma. The paragenesis of each type of
uraninite analyzed is shown in Figures 2.8 and 2.9 and described in Section 4.3.
63

Regression to zero content of the sum SiO 2 and Fe 2 O 3 in the Athabasca-related U 6
uraninite gives a Chemical Pb age of 1619 Ma (Fig. 2.12D). This age overlaps the upper
intercept age of 1601±64 Ma and the 207 Pb/ 206 Pb age of 1620±4 Ma (Fig. 2.11F) and is
interpreted as the formation age of ±U 6 uraninite.
The higher degree of alteration of U 3 uraninite associated with the granite-related
metasomatic-type mineralization in Gunnar, as indicated by the much lower Pb contents
and the higher total silicate elements, is reflected by much lower Chemical Pb ages (Table
2.3). These ages range from 164 Ma to 0 and reflect recent alteration of U 3 uraninite in
Gunnar, which is also reflected by the low Pb/Pb and U-Pb ages (Tables 2.1 and 2.2).
64

Figure 2.12. Plot of element contents in uraninite as a function of chemical Pb ages. A: Early
tensional vein type ±U 2 uraninite (Sample 6122BV-Cat, Ace deposit) . B: Breccia-type U 4
uraninite (Sample B5812, Ace-Fay deposit). C: Volcanic-type ±U 5 uraninite (Sample B6120,
Ace-Fay deposit). D: Athabasca-related ±U 6 uraninite (Sample B3705, Ace-Fay deposit).
2.5. DISCUSSION
2.5.1. Interpretation of the Main Ore shear zone and Saint Louis fault
Structural and textural relationships along the Main Ore shear zone and the Saint
Louis fault indicate a sequential development of early ductile and ductile-brittle, to late
brittle episodes of movement (Fig. 2.13). The Main Ore shear zone and the Saint Louis fault
display a spatial distribution of deformed rocks that is consistent with a dominant
extensional normal sense of movement (Sibson, 1977). Therefore, the Main Ore shear zone
is interpreted as an oblique-normal and dextral listric fault. The sense of movement along
the Saint Louis fault is contentious due to paucity of shear sense indicators. Allen (1963)
described the Saint Louis fault as a dextral normal fault with multiple slip events. However,
the footwall-dominated mylonite and the hanging wall-dominated cataclasite, which is
capped by the Martin Lake basal conglomerate, suggest a significant normal sense of
movement.
Metamorphic relationships indicate that mylonitization was initiated in the ductile
environment (Fig. 2.13B) at amphibolite metamorphic conditions and that retrogression to
lower greenschist facies is concomitant with exhumation to shallower crustal depths. The
host mylonites are overprinted by ductile-brittle and brittle faults, reflecting progressive
unroofing of the shear zones to shallower crustal levels. The ductile shear zones
experienced reactivated slip movement in the ductile-brittle zone associated with cataclasite
65

faults (Fig. 2.13C). The breccias were generated later at a shallow level in the brittle
environment (Fig. 2.13E). The shear zone is further cut by more brittle features associated
with veins and dikes (Figs. 2.13F and 2.13G).
The Main Ore shear zone and the Saint Louis fault display evidence for hydration
and fluid flow. Retrograde metamorphism following mylonitization involved exothermic
hydration reactions evidenced by the presence of en-échelon quartz-filled tension gashes
(Fig. 2.5G), tensional veins (Fig. 2.9B), hydraulic breccia (Fig. 2.5L) and chlorite, calcite
and albite veins (Fig. 2.7H) that occur within these shear zones. All the evidence suggests
that hydration associated with fluid circulation prevailed during the development of the
shear zones and played a key role in the alteration and ore-forming processes.
Petrographic, paragenetic mineral and ore alteration relationships, together with
geochronological data and the various deformation features within the Main Ore shear zone
and Saint Louis fault indicate six events of uranium mineralization. These are related to
episodic brittle reactivation of the fault zones (Fig. 2.8) that create dilatant areas, which are
favorable structural sites for fluid flow, hydrothermal alteration, and uranium
mineralization.
Sediments of the Murmac Bay Group were deposited in a tectonically active
extensional fault-bounded Paleoproterozoic Basin (Ashton et al., 2009b) (Fig. 2.13A). Slip
activity along fault zones was likely initiated shortly after deposition of the Murmac Bay
sediments at ca. 2.33 Ga (Hartlaub et al., 2004; Ashton and Hartlaub, 2008). The Group is
intruded by the ca. 2.33–2.30 Ga ‘North Shore Plutons’ (Macdonald et al., 1985) likely
related to tectonic extension during the Arrowsmith Orogen (Hartlaub et al., 2007). The
66

plutons include the 2321±3 Ma Gunnar granite (Fig. 2.13B) (Hartlaub et al., 2007), which
hosts the granite-related metasomatic-type U 3
uranium mineralization. Crosscutting
relationships suggest that the metasomatic-type mineralization pre-dates the breccia event.
The timing of U 3 -mineralization is therefore constrained between the age of the Gunnar
granite and the age of the breccia that has overprinted the U 3 -mineralized granite.
Deposition of the Murmac Bay Group, Mylonitization and Granitization
Various periods of tectonic reactivation, basin formation, volcanism and uranium mineralization
67

Figure 2.13. Schematic cross-sections illustrating the general tectonic evolution and timing of
the uranium mineralization in the Beaverlodge area. A: ≈2.33 Ga: Deposition of the Murmac
Bay Group rocks in a tectonically active fault-bounded Paleoproterozoic basin. B: ≈2.33-2.3
Ga: mylonitization with oblique-normal and dextral sense of shear along fault zones,
concomitant with emplacement of the Gunnar granite. C: 2.29 Ga: Reactivation during late
Arrowsmith orogenic exhumation. Cataclasite fault overprinted the mylonite. ±U1 is
68

associated with cataclasite rocks. Hydraulic fracturing in response to fluid generation via
decompression and hydration reactions was probably the mechanism of the early tensional
±U2 veins formation. D: 2.0-1.9: 1.94-1.92 Ga peak metamorphism of the Taltson-Thelon
Orogen produced a regional migmatitic foliation (S1) and tight to isoclinal folds of early S1
fabric. 1.91-1.90 Ga metamorphic event of the Snowbird Tectonic Zone produced an
overprinting northeast-striking regional fabric associated with tight to isoclinal folds. E: 1850
Ma: U4-rich brecciation of pre-existing rocks along reactivated faults during regional
metamorphism of the Trans-Hudson Orogen or most likely post-peak compressional uplift
during terminal collision of the Taltson-Thelon Orogen. F: 1820 Ma: Formation of the
successor Martin Lake Basin, which developed along lines of pre-existing tectonic weakness
during late stage of the Trans-Hudson Orogen. The Martin Lake Basin is associated with
extrusion of mantle-affinity alkaline to sub-alkaline mafic dikes around 1818±4 Ma. The
volcanic-type ±U5 is spatially associated with the mafic dikes. G: 1620 Ma: Deposition of the
Athabasca Basin at ca. 1750 Ma and formation of Athabasca-related ±U6 veins coincident
with the age of the unconformity-related U-mineralizing event in the Athabasca Basin that
records tectonic reactivation during the 1.65-1.60 Ga Mazatzal Orogen. H: Late alteration
events: From the Mesoproterozoic to recent time, far field tectonic events of several orogenic
episodes during the thermotectonic evolution of the Laurentian plate caused minor brittle
fault reactivation in the Beaverlodge area.
2.5.2. Temporal relationships of fault activities and uranium mineralization to
regional tectonic events
The oldest observed deformation event corresponds to mylonitization with obliquenormal
and dextral sense of shearing in the ductile environment at amphibolite facies
metamorphism (Fig. 2.13B). Mylonitization along these faults likely occurred during the
Arrowsmith Orogen at ca. 2.33 Ga (Berman, 2005; Hartlaub et al., 2007), concomitant with
initial deposition of the Murmac Bay Group sediments. Metamorphic retrogression took
place during exhumation to shallower crustal depths, resulting in greenschist facies
conditions, probably subsequent to a period of tectonic quiescence and regional erosion.
69

Mylonites were then reactivated at shallower structural levels where brittle-ductile
fracturing under hydrated conditions associated with cataclasite faulting became the
dominant failure process (Fig. 2.13C).
The formation age of the cataclasite ±U 1 and early tensional veins-type ±U 2
mineralization, suggests that these two mineralizing events were coeval and their timing is
consistent with fault reactivation during late stage Arrowsmith Orogen that affected the
Beaverlodge area (Fig. 2.13C). Post-orogenic exhumation and erosion may have led to the
development of fluid-related features (Miller et al., 2002) as deformation occurred under
hydrated conditions in the ductile-brittle environment. Hydraulic tensile fracturing in
response to fluid generation via decompression and hydration reactions (Miller and
Cartwright, 2006) was probably the mechanism of the early tensional ±U 2 -veins formation.
The vein-forming fluid was likely driven into these fractures by suction pump processes
(Sibson, 1987). Interaction between the hydrothermal brine and the metamorphic host rocks
likely promoted the deposition of the ±U 2 uranium mineralization and the Cal 2 -Hem 3 -Chl 3 -
Src 2 -Cpy 2 -Py 2 mineral assemblage (Fig. 2.8).
The 207 Pb/ 206 Pb system of U 1 and U 2 uraninites displays five groups of ages reflecting
post-mineralization alteration by later fluid events that are related to fault reactivation (Fig.
2.15). The intervals 2.2-2.1 Ga and 2.1-2.0 Ga correspond to a period of global extension
and rifting related to the protracted breakup of the Kenorland supercontinent (Williams et
al., 1991; LeCheminant et al., 1997) (Fig. 2.15). For example, the 2.2-2.1 Ga mafic swarms
in the Slave, Churchill, Superior and Nain provinces (LeCheminant et al., 1996; Bleeker et
al., 2007) and the 2.2-2.0 Ga intrusive complexes in the Slave province (Buchan and Ernst,
70

2004) are all interpreted as related to Kenorland breakup. The 2.0-1.9 Ga period is
consistent with the compressional Taltson-Thelon Orogen (Henderson et al., 1990; Chacko
et al., 2000) and Snowbird Tectonic Zone (Baldwin et al., 2003, Berman et al., 2007a), in
the west and east of the Beaverlodge area, respectively (Fig. 2.14).
Figure 2.14. Regional geological map of the North American shield showing lithotectonic
units, the major orogenic phases and the Beaverlodge location. The map also show the Trans-
Hudson orogen surrounded by the Wyoming, Slave, Hearne, Rae and Superior cratons that
constitute the central core of the North American craton (Laurentia) (modified from
Hoffman, 1988).
The Thluicho Lake Group, a fining-upwards, conglomerate–arkose–argillite
succession located west of the Beaverlodge area, deposited in an intermontane setting
towards the end of the Taltson Orogen (Ashton et al., 2009a). Bethune et al. (2010)
interpreted the first stage of folding as associated with a north-northeast-directed folding
71

and thrusting during the 1.94-1.92 Taltson-Thelon Orogen, producing tight to isoclinal
folds, ductile transposition and development of east-southeast-trending foliation superseded
by north-northwest-trending upright folds. This is consistent with F1, F2 and F3 type 2
interference fold pattern observed at the Ace-fay deposits (Fig. 2.7D). Ashton et al. (2007)
interpreted overprinting tight to isoclinal northeast-trending, predominantly southwestplunging
folds that formed during the 1.91-1.90 Ga metamorphic event of the Snowbird
Tectonic Zone (Fig. 2.15). These two major compressional orogens (Fig. 2.13D) likely
overprinted and obscured early ductile and brittle-ductile fabric associated with the
Arrowsmith Orogen.
Subsequent to a period of erosion that exposed the fault zones at shallower crustal
levels immediately after the Snowbird Tectonic Zone (Bethune et al., 2010), fault activity
changed from dominantly ductile-brittle to brittle deformation causing widespread U 4
uranium-rich brecciation along reactivated fault zones (Fig. 2.13E). The 1848±5 Ma U 4
uranium-brecciation stage is consistent with fault reactivation during tectonic shortening
and regional metamorphism of the Trans-Hudson Orogen or more likely post-peak
compressional uplift during terminal collision of the Taltson-Thelon Orogen. Reactivated
fault zones would have acted as high-permeability conduits that focus fluid flow into the
breccia system leading to hydrothermal alteration and deposition of the U 4 uranium
mineralization and Br 1 -Chl 7 -Src 3 -Hem 6 -Py 5 -Cpy 4
mineral assemblage (Fig. 2.8). The
Trans-Hudson Orogen, located east of the Beaverlodge area (Fig. 2.14), marks the
amalgation involving Wyoming, Slave, Churchill, Superior and Sask provinces into the
cratonic core of Laurentia (Hoffman, 1989; Ansdell, 2005). Ansdell et al. (1999) identified
72

a ca. 1.85-1.83 Ga event associated with a northwest subduction that reactivated an earlier
northwest-dipping suture beneath the La Ronge-Lynn Lake arc. The 1848±5 Ma main
breccia-related U 4 uranium mineralization could be related to fault reactivation during the
ca. 1.85-1.83 Ga event in the Trans-Hudson Orogen.
Southeastward underthrusting of the Rae-Hearne foreland under the Superior
hinterland during the ca. 1.83-1.81 Ma terminal collision of the Trans-Hudson Orogen
(Ansdell and Yang 1995; Ansdell et al., 1999) is interpreted to have caused intracratonic
deformation and significant extension in the Rae back-arc and formation of the 1820 Ma
successor Martin Lake Basin (Mazimhaka and Hendry, 1985), which developed along lines
of pre-existing tectonic weakness (Fig. 2.13F). The plate-scale tectonic setting of this basin
is more compatible with an extensional rift regime, which is consistent with geodynamic
models that suggest subduction initiation followed by rapid back-arc extension and basin
formation (McKenzie, 1978; Clendenin et al., 1988). Ashton et al. (2009b) suggested that
brittle–ductile to brittle trans-tensional faulting at the junction of the Black Bay (Bergeron,
2001, 2002) and Saint Louis faults (Fig. 2.2) created a small pull-apart basin into which the
Martin Lake Basin was deposited. The Martin Lake Basin is associated with extrusion of
mantle-affinity alkaline to sub-alkaline mafic dikes at 1818±4 Ma (Morelli et al., 2009).
Magma ascended during extensional reactivation of deep fault zones, which act as conduit
for intrusion of the mafic dikes (Fig. 2.13F). Magmatic-hydrothermal degassing through
preexisting fractures and joints is likely related to the volcanic-related U 5 uranium
mineralization and associated mineral assemblage (Fig. 2.8). The 1812±15 Ma U 5 -
mineralization coincides with the 1818±4 Ma Martin Lake mafic volcanism in the
73

Beaverlodge area (Morelli et al., 2009) (Fig. 2.15). These ages are identical to an 1827±4
Ma age (Bostock and Breemen, 1992) obtained for the southeast-east-southeast-striking
Sparrow diabase dike swarms, which span the boundary between the Taltson Magmatic
Zone and the western Churchill province (Fig. 2.14). These dates are also similar to the
1800 Ma age that Russel and Ahren (1957) reported for the west orebody of the Ace
deposit (Fig. 2.2). The U-Pb upper intercept ages of 1783±7 Ma and 1774±25 Ma (Figs.
11D and 11E) are identical to the 1780±20 Ma date that Koeppel (1969) originally
interpreted as the age of vein-type uranium deposits in the Beaverlodge area. However,
these ages are likely related to a post-mineralization alteration and resetting event
associated with fault reactivation during the emplacement of the 1788±3 Ma (Ashton et al.,
2009b) northeast-striking, post-orogenic, lamprophyre and granitic dikes (Sassano et al.,
1974; Ashton et al., 2006) that cut the Uranium City mafic dikes (Tremblay, 1972).
Sassano et al. (1974) suggested that the lamprophyre dikes are associated with the latekinematic
phase of the Trans-Hudson Orogen, at which time the uplift of the northwest
Churchill province took place.
Late east-west compressional regime associated with tectonic readjustments during
terminal ca. 1.81-1.69 Ga post-collisional convergence in the Trans-Hudson Orogen (e.g.
Hajnal et al., 1996; Chiarenzelli et al., 1998) caused folding of the Murmac Bay Group and
Martin Lake Basin rocks (Ashton et al., 2009a), followed by uplift, erosion, thermal
relaxation, subsidence, and deposition of the Athabasca Basin at ca. 1750 Ma (Kyser et al.,
2000) (Fig. 2.13G). Late brittle reactivation along fault zones during the Mesoproterozoic
caused minor fracturing and deposition of U 6 uranium mineralization related to fluids likely
74

originating from the Athabasca Basin and descended downward along reactivated fracture
systems in the basement rocks. Interaction between the hydrothermal brine and the
metamorphic basement lithologies may have led to the deposition of the ±U 6 uranium
mineralization and Cal 10 -Chl 9 -Hem 8 -Py 7 mineral assemblage (Fig. 2.8). The 1620±4 Ma
Athabasca-related ±U 6 uranium mineralization is coincident with the age of the major
unconformity-related uranium mineralizing event in the Athabasca Basin (Alexandre et al.,
2007) and records tectonic reactivation during the 1.65-1.60 Ga Mazatzal Orogen in
southern Laurentia (Fig. 2.14) (Labrenze and Karlstrom, 1991; Eisele and Isachsen, 2001).
The Athabasca-related U 6 uranium mineralization age is also within the 1700-1500 Ma
intervals that Robinson (1955) originally suggested as the earliest uranium mineralization
in the Beaverlodge area.
From the Mesoproterozoic to recent time (Fig. 2.13H), far field tectonic events of
several orogenic episodes during the thermotectonic evolution of the Laurentian plate (e.g.
Hoffman, 1989; Evans and Pisarevsky, 2008) caused minor brittle fault reactivation in the
Beaverlodge area (Fig. 2.15). Post-mineralization alteration for all stages of uraninite
record a Mesoproterozoic tectonic event at ca. 1.4 Ga (Fig. 2.15), which corresponds to the
Granite Pluton event (1.55-1.35 Ga) along the southeastern margin of Laurentia (Fig. 2.14)
(Barinek et al., 1999; Thompson and Barnes, 1999). This event is subsequent to the final
breakup of the Nuna supercontinent (Hou et al., 2008; Evans et al., 2010) that culminated
at ca. 1.3 to 1.2 Ga (Ernst et al., 2008). The metasomatic-type U 3 uraninite in Gunnar
records this breakup event at ca. 1.27 Ga (Fig. 2.15), similar to the 1.27 Ga Mackenzie
75

dikes (Ernst and Buchan, 2001b) and the 1.24 Ga Sudbury mafic dikes (Dudás et al., 1994)
that are associated with the Nuna supercontinent breakup (Rogers and Santos, 2002).
The breccia-type U 4 and metasomatic-type U 3 uraninites record 400 Myr of alteration
extending from 1.3 to 0.9 Ga (Fig. 2.15), which likely corresponds to the protracted period
of Rodinia supercontinent assembly (Piper, 2000, 2004, Li et al., 2008) through the
Grenville Orogen (Rivers, 1997; Carr et al., 2004). This orogenic activity along the
southern margin of Laurentia (Fig. 2.14) culminated into continent-continent collision that
led to the final Rodinia assembly (Moores, 1991; Bogdanova et al., 2009).
The metasomatic-type U 3 and breccia-type U 4 uraninites show intense alteration at
800-780 Ma and 550-500 Ma (Fig. 2.15). These ages are consistent with diachronous
breakup models of Rodinia (Dalziel, 1991; Moores, 1991; Li et al., 2008), comprised of an
early rifting stage along the western margin of Laurentia at ca. 780-755 Ma (Harlan,
2003b) followed by the main pulse of rifting along the eastern margin at ca. 600-550 Ma
(Ernst and Buchan, 2001b). Mafic intrusions associated with this major extensional event
occur along the western margin of Laurentia (Fig. 2.14) and include the ca. 780-770 Ma
Gunbarrel mafic event (Harlan et al., 2003b). The ca. 570-550 Ma central-Iapetus mafic
intrusion along the eastern margin of Laurentia occurred during Rodinia eastern breakup
(Kamo et al., 1989; Li et al., 2008).
All uraninite types have been affected by alteration between 460 Ma and 280 Ma,
with peaks at ca. 350 Ma (Fig. 2.15) recording the thermotectonic event of the protracted
Appalachian Orogen that affected the eastern margin of Laurentia (Fig. 2.14) during
Pangea assembly (Cocks and Torsvik, 2002; Hatcher, 2002).
76

U-Pb isotopic systems have lower intercept ages reflecting post-Appalachian tectonic
history of the North American shield. These ages range from 166±30 Ma to 54±87 Ma
(Tables 2.1b and 2.2b) and likely reflect tectonic activity during the Cretaceous and
Paleocene Cordilleran orogenic belt of North America (Molnar and Atwater, 1978). The
belt marked by a zone of strong folding and thrust faulting is located further east of the
Beaverlodge area, along the western active margin of Laurentia (Fig. 2.14).
77

Figure 2.15: Distribution of 207 Pb/ 206 Pb ages for 260 uraninite grains along with the timing of
various uranium mineralization and tectonic events that affected the Beaverlodge area. The
ages are from analysis of grains from different styles of uranium mineralization. Also shown
are the area distribution of supercontinents and major magmatic events in North America.
(e.g Hoffman, 1989; Ernst and Buchan, 2001b; Li et al., 2008)
Lower U-Pb intercept and chemical Pb ages close to 0 Ma (Tables 2.1, 2.2, and 2.3)
are interpreted to record recent fault reactivation and resetting events likely during the
Pleistocene glaciations-related stress fluctuation that caused continental-scale isostatic
readjustments as the upper crust deformed in response to deglaciation and lithospheric
unloading (Adams, 1989; Karlstrom, 2000; Fullerton et al., 2003). Similar ages are also
recorded in uranium deposits in the Athabasca Basin (Alexandre et al., 2005).
These alteration and resetting stages of uraninites and the late Chl 9 , Cal 11 , Qtz 5 and
Hem 9 veins that cut across the fault zones record the effect of late fluid events that have
affected the deposits subsequent to their formation. The late fluid events may represent
incursion and circulation of hydrothermal and meteoric water through the structurally
reactivated fault zones (Kotzer and Kyser, 1995), suggesting that the fault zones were
active after deposition of the uranium mineralization and remain zones of preferential fluid
circulation (Fayek and Kyser, 1997).
2.6. CONCLUSIONS
Structural and metamorphic relationships within the Main Ore shear zone and the
Saint Louis fault, and petrographic analysis and geochronological data from various
uranium deposits indicate that the Beaverlodge area records ore-forming systems that
result from a complex history of multiple reactivation and hydrothermal alteration
78

processes during continent-scale protracted tectonic evolution. Stages of uranium
mineralization and alteration events record over 2.3 Gyrs of tectonic history of the North
American shield. Results presented indicate that uraninite in major structures is greatly
sensitive to fluid events stimulated by both near- and far-field tectonic events. Therefore, it
can serve as vehicle to understand the complex timing relationships between fault
activities, hydrothermal and ore-forming processes, to regional thermotectonic events.
Six distinct stages of uranium mineralization associated with multiple postmineralization
alteration events are identified. The main event that hosts most of the
uranium mineralization occurred during the Trans-Hudson Orogen or more likely postpeak
Taltson-Thelon Orogen and is associated with far-field fault reactivation. This
deformational event produced widespread uranium-rich breccia zones that overprinted
early ductile and brittle-ductile shear zones and are the primary structural control for
uranium mineralization. Exploration activities should therefore be focused in areas of fault
zones that demonstrate evidence of tectonic reactivation that create dilatant areas, which
are favorable structural sites for fluid flow, hydrothermal alteration, and uranium
mineralization.
79

CHAPTER 3
GENESIS OF MULTIFARIOUS URANIUM MINERALIZATION IN
THE BEAVERLODGE AREA, NORTHERN
SASKATCHEWAN, CANADA
Abstract
The Beaverlodge area in northwestern Saskatchewan, Canada, hosts numerous faultcontrolled
U deposits that are geochemically and structurally complex because of multiple
deformation, hydrothermal alteration and U mineralization events. Field and petrographic
studies combined with electron microprobe analysis, stable isotope geochemistry of H, C,
O, as well as geochronological data have identified up to six temporally distinct stages of
U mineralization. Early minor stages are hosted in cataclasite and veins at ca. 2.29 Ga and
in albitized granite in the Gunnar deposit between ca. 2.3 Ga and 1.9 Ga, which predate
the main stage of U mineralization as hydrothermal breccias that formed at ca. 1.85 Ga.
Later stages of U mineralization are related to minor veins at ca. 1.82 Ga linked to alkaline
mafic dikes associated with the Martin Lake Basin and to minor veins at ca. 1.62 Ga
corresponding to the timing of unconformity-type uranium mineralization in the
Athabasca Basin.
Early vein and cataclasite-type mineralization formed during late stages of the early
Paleoproterozoic Arrowsmith Orogen and represent the earliest recorded fluid events.
Stable isotope geochemistry of C and O of syn-ore calcite and syn-ore chlorite crystal
chemistry indicate that the early veins formed from fluids derived from retrograde
metamorphic processes at 310 o C. Granite-related metasomatic-type mineralization at
80

Gunnar formed from reducing hydrothermal brines that exsolved from magmatic fluid at
315 o C. However, uranium associated with this metasomatic style of mineralization is
overprinted by the more significant breccia-vein and later, minor volcanic-type
mineralizations. The Gunnar deposit contains all three styles of mineralization.
During the Paleoproterozoic, reactivation of major fault zones is related to the
dominant breccia-type mineralizing event. Syn-ore chlorite crystal chemistry and stable
isotope geochemistry of H, C, and O of syn-ore minerals indicate that the main U-
mineralizing event at 1.85 Ga in all deposits in the Beaverlodge area, formed from Ca-Na-
F-rich fluids at 330 o C associated with regional metamorphism coincident with the postpeak
Thelon-Taltson Orogen or, more likely, early stages of the Trans-Hudson Orogen.
During the late Paleoproterozoic, formation of the Martin Lake Basin and associated
volcanic rocks is related to the volcanic-type mineralization at 1.82 Ga. Syn-ore chlorite
crystal chemistry and stable isotope geochemistry of H, C, and O of syn-ore minerals
indicate that this mineralization formed at 320 o C from magmatic fluids originating from
the alkaline mafic dikes. The last stage of mineralization formed at ca. 1.62 Ga from
oxidizing basinal brines at 235 o C originating from the Athabasca Basin. Subsequent
erosion of the Athabasca and Martin Lake Basin rocks and weathering of the deposit
resulted in the formation of secondary uranium minerals and late veins.
These results improve the current genetic model for uranium mineralization in the
Beaverlodge area to a level that takes into account the multiple stages of deformation and
fluid overprinting that occurred over a period of at least 2.3 Gyrs. Although the
Beaverlodge area represents several distinct mineralizing events, the major event is the
81

eccia-type. The other styles of mineralization are minor, and their presence complicates
both exploration and our understanding of deposit genesis in the area.
3.1. Introduction
The Martin Lake successor basin (Hendry, 1983; Mazimhaka and Hendry, 1985), in
the Beaverlodge district, Saskatchewan, Canada, was affected by a protracted history of
deformation, hydrothermal alteration and uranium mineralization during the Proterozoic
(Dieng et al., 2011). Despite several decades of intense exploration and mining activities,
only limited studies of the fluid characteristics of a few deposits have been reported (e.g.
Robinson, 1955; Beck, 1969; Sassano et al., 1972; Hoeve, 1980, 1982; Sibbald, 1982;
Rees, 1992; Kotzer and Kyser, 1995). Therefore, the key processes by which these
deposits formed remain largely unknown. The U mineralization occurs in basement rocks
beneath, and within, the Paleoproterozoic Martin Lake Basin (e.g. Tremblay, 1968;
Sassano, 1972; Slater, 1983) that is stratigraphically older than, but spatially related to the
U-rich Athabasca Basin (Kyser et al., 2000; Alexandre et al., 2009). However, whether or
not these deposits are unconformity-related and how they are related to those in the
Athabasca Basin is moot.
In this chapter, we evaluate the character and formation of uranium deposits in the
Beaverlodge area using mineral paragenesis that details the relative timing of alteration
minerals. We also constrain the nature and origin of fluids in equilibrium with these
minerals by using stable isotope geochemistry, rare earth element contents in uraninite,
and chlorite and uraninite crystal chemistry. These results are used to identify key factors
controlling U mineralization in the Martin Lake successor basin, present a conceptual
82

genetic model for the different styles of U mineralization in the Beaverlodge area, and
compare the Beaverlodge U deposits to those in the younger, U-rich Athabasca Basin.
3.2. Geologic Setting
3.2.1. General geology
The Beaverlodge area lies within the southwestern Rae province (Fig. 3.1) and
comprises Neoarchean to Mesoproterozoic rocks that can be broadly divided into four
packages (Fig. 3.2).
Location Map
Study area
Uranium deposits
Figure 3.1. Generalized geological map of the Western Churchill Province, Canada, showing
lithotectonic units, uranium deposits and location of the Beaverlodge area. (modified from
Hoffman, 1988).
83

The basement consist of Neoarchean granitoids (Ashton et al., 2004) including the
Elliot Bay (3014 Ma; Persons, 1983), Lodge Bay (3060 Ma; O’Hanley, et al., 1991) and
Cornwall Bay (2999 Ma; Hartlaub et al., 2004a) granites. The overlying Neoarchean to
Paleoproterozoic supracrustal Murmac Bay Group (Hartlaub and Ashton, 1998; Hartlaub
et al., 2004a) is composed of metamorphosed and moderately to highly deformed
supracrustal rocks consisting of a basal quartzite, basalt, ultramafic to intermediate
igneous rocks, and psammite and pelite with minor amounts of conglomerate, banded iron
formation, and carbonates rocks (Hartlaub and Ashton, 1998; Ashton et al., 2004). The
Murmac Bay Group was variably metamorphosed from granulite facies to lower
greenschist facies (Hartlaub and Ashton, 1998). Recent work indicates that the basal
quartzo-feldpathic units of the Murmac Bay Group have a maximum depositional age of
2.33 Ga (Hartlaub et al., 2004a). The Murmac Bay Group is intruded by a suite of ca.
2.33–2.30 Ga granites known as ‘North Shore Plutons’ (Macdonald et al., 1985) including
the 2321±3 Ma Gunnar granite (Hartlaub et al., 2004a) that is associated with a major U
deposit in the Beaverlodge area (Fig. 3.2). The tectonic environment of the plutonic suite
and the depositional setting of the Murmac Bay Group and their timing relationships to
deformation are still poorly understood.
84

Figure 3.2. Simplified geological map of the Beaverlodge area showing the location of the
studied uranium deposits. (modified from Macdonald and Slimmon, 1985).
The Paleoproterozoic Martin Lake Basin (Fig. 3.2) is a ca. 5000 m-thick, molasse,
red-bed succession (Langford, 1981; Mazimhaka and Hendry, 1985; Morelli et al., 2001)
85

of essentially unmetamorphosed arkose, conglomerates and siltstone with mafic flows and
sills of alkaline affinity (Morelli et al., 2009). The fault-controlled basin is confined to a
broad open syncline centered on Martin Lake (Ramaekers, 1981; Ashton et al., 2001).
Locally, extensive suites of east- to southeast striking mafic dikes, dated at 1818±4 Ma,
are interpreted as feeders to the Martin Lake Basin mafic flows and sills (Morelli et al.,
2009). The Martin Lake Basin formed during a period of active tectonism related to backarc
extension (Dieng et al., 2011) following the peak Trans-Hudson Orogeny (Hoffman,
1989, 1990; Corrigan, 2009) and can be therefore classified as a successor basin
(Clendenin et al., 1988).
Overlying the Martin Lake Basin are outliers of the Paleoproterozoic to
Mesoproterozoic Athabasca Formation (Rainbird et al., 2007). These occur south of the
Beaverlodge area and consist of generally flat-lying, undeformed quartz sandstone with
minor shale, conglomerate, and greywacke (Sibbald, 1983).
3.2.2. Uranium mineralization
The Beaverlodge area hosts a multitude of U deposits (Fig. 3.2), which were
actively mined between 1953 and 1963 from 284 deposits. Ore grades were generally in
the range of 0.15 to 0.25 per cent U but in places, up to 0.4 per cent U (Robinson, 1955;
Beck, 1969). About 25,000 t U was mined (Sibbald and Quirt, 1987), which is the
equivalent of the Millennium deposit in the Athabasca Basin (Roy et al., 2005). Some
previous investigators of the Beaverlodge U deposits reported a single event of U
mineralization (Dudar, 1960; Sassano, 1972), but others described two mineralizing
events (Turek, 1962). However, Tortosa (1983) identified five stages of U mineralization
86

separated by fracturing events in the Cenex deposit that is located east of the Cinch Lake
deposit. Joubin (1955) and Johns (1970) proposed a surficial origin for U mineralization
and suggested that most of the pitchblende occurrences formed near the unconformity
between the Tarzin and Martin Lake groups. Sassano et al. (1972) proposed a
metamorphic hydrothermal source for the fluids and U based on studies of the Eldorado
mine, wherein the deposits were generated by pore fluids in the supracrustal rocks and
remobilized during metamorphism. Tortosa (1983) proposed a groundwater source for the
mineralizing fluids that circulated through fracture zones near the surface and leached U
from rocks to form the orebody at temperatures near 250 o C. Isotopic and
microthermometric studies on silicate, carbonate, and oxide gangue minerals associated
with U-oxide minerals from the Athabasca Basin and Beaverlodge area indicate that fluids
involved with formation of unconformity-type and complex vein-type U mineralization
were saline (10-40 wt % NaCl) having δ 18 O values ranging from -27 to -3 per mil and
temperatures between 150 o C and 220 o C, but variably overprinted by relatively modern
meteoric fluid processes (Peiris and Parslow, 1988; Kotzer and Kyser, 1995).
3.3. Methodology
Polished thin sections were prepared for 550 samples from outcrop and core of most
of the major deposits (Fig. 3.2) and were examined using transmitted and reflected-light
microscopy to determine mineral crosscutting relationships and develop a detail
paragenesis for the Beaverlodge district (Fig. 3.3).
Electron microprobe analysis of syn-ore chlorite and uraninite were accomplished
on polished thin sections using a Cambax MBX electron microprobe equipped with 4
87

WDX X-ray spectrometers at Carleton University, Ottawa, Canada. A suite of natural and
synthetic minerals were used as calibration standards. The Cameca PAP matrix correction
program was used to convert the raw X-ray data into elemental weight percent. The
detection limit for the majority of the elements is ca. 0.05 percent and the accuracy of the
measurements is 2% relative for major elements and 5% relative for minor elements. The
crystal chemistry of paragenetically distinct chlorites was used to estimate their formation
temperatures using the chlorite geothermometry of Cathelineau (1988). For uraninite,
UO 2 , SiO 2 , CaO, Fe 2 O 3 , TiO 2 , Cr 2 O 3 , V 2 O 5 , PbO, P 2 O 5 , K 2 O ThO 2 , MnO, Y 2 O 3 , Tb 2 O 3 ,
and CuO were measured to determine their chemical compositions.
Clay minerals were extracted by ultrasound disintegration and centrifugation and
analyzed by X-ray diffraction (XRD) using a Siemens X-pert instrument at Queen’s
University, Canada. Monomineralic fractions, typically > 95 percent pure, were used for
stable isotope analysis at the Queen’s Facility for Isotope Research (QFIR). Oxygen
isotopic compositions of chlorite were measured using the BrF 5 method of Clayton and
Mayeda (1963) and a dual inlet Finnigan MAT252 isotope ratio mass spectrometer.
Hydrogen isotopic compositions were determined using a Thermo Finnigan TC/EA in-line
with a DeltaPlus XP Finnigan Mat mass spectrometer. Isotopic compositions are reported
in the δ notation in units of per mil relative to V-SMOW. Analyses of δ 18 O were
reproducible to ±0.2 per mil and δ 2 H values were reproducible to ±3 per mil. The isotopic
composition of fluid was calculated using the chlorite–water fractionation factor of
Wenner and Taylor (1971) for oxygen and the chlorite–water fractionation factor of
Marumo et al. (1980) for hydrogen.
88

Stable isotopic compositions of C and O in calcite and dolomite were made using a
Gas Bench coupled to a ThermoFinnigan Delta plus XP mass spectrometer and are reported
in the δ notation in units of per mil relative to V-PDB and V-SMOW, respectively. The
isotopic compositions of C and O in the fluid were calculated from the fractionation factor
of Ohmoto and Rye (1979) and Hu and Clayton (2003), respectively.
The content of REEs in uraninite was determined by LA-ICPMS using a
ThermoFisher X-Series II. This instrument is equipped with a New Wave UP-213
Nd:YAG laser-ablation system using a small volume (2.5 cm 3 ) and laminar-flow
SuperCell ablation cell. Ablation was performed in an atmosphere of pure He (0.6
l/min), with the ablated aerosol mixed with Ar (0.8 l/min) immediately after the ablation
cell and prior to direct introduction into the torch. Pre-defined areas of the polished thin
sections were ablated using a spot size of 30μm in diameter. Instrument drift was
performed using NIST 612 and calibration was performed using zircon standard 91500
(Wiedenbeck et al., 1995). The REE abundances are normalized to the abundances in
chondrite meteorites reported by McDonough and Sun (1995). Heavy and light REE
variations are reflected by chondrite normalized (La/Yb) N , (La/Sm) N and (Tb/Yb) N ratios,
whereas redox conditions are recorded by Eu/Eu* and Ce/Ce* anomalies (DeBaar, 1991;
Gao and Wedepohl, 1995).
Mineral name abbreviations used in this chapter are those from Kretz (1983). The
superscript numerical value on mineral name abbreviations reflects the mineral growth
stage.
89

3.4. Results
3.4.1. Paragenesis of the alteration minerals and types of U mineralization
The paragenetic mineral assemblage is based on detailed petrographic analysis of
550 samples collected from the Ace-Fay, Gunnar and Cinch Lake deposits and on field
relationships. These deposits are the largest in the Beaverlodge area (Fig. 3.2). There are
six mineralogically, temporally, and structurally distinct U ore and related alteration
assemblages within the U deposits in the Beaverlodge area (Figs. 3.3 and 3.4).
Mylonitization is the earliest deformation observed (Dieng et al., 2011). The
hornblende-feldspar gneiss at Cinch Lake and the Foot Bay gneiss at Ace-Fay define an
amphibolite metamorphic assemblage of Kfs 1 +Pl 1 +Hbl 1 . Retrogression to greenschist
metamorphic grade is indicated by the assemblage Bt 1 +Chl 1 +Src 1 +Hem 1 (Fig. 3.3). The
mylonitic foliation is cut by Chl 2 chlorite, Qtz 2 quartz, Ab 1 albite, Cal 1 calcite, and Ep 1
epidote veinlets (Fig. 3.3). The mylonites are further overprinted by a network of ductilebrittle
and brittle features that host the U mineralization (Dieng et al., 2011). The
cataclasite comprises mylonite fragments (Fig. 3.4A), Qtz 1 quartz and Kfs 1 feldspar clasts,
and disrupted Cal 1 calcite and Qtz 2 quartz veinlets embedded in a matrix composed of
recrystallized Qtz 1 quartz, Cal 2 calcite, Hem 3 hematite, Chl 3 chlorite, Src 2 sericite, and
disseminated U 1 uraninite (Fig. 3.4B). Cataclasite rocks are occasionally cut by tensional
Qtz 3 quartz-Cal 3 calcite and U 2 uraninite veins (Fig. 3.4C). Fine-grained Cal 4 calcite, Chl 4
chlorite, Hem 4 hematite, and Py 3 pyrite are intergrown with U 2 uraninite (Fig. 3.4D). Qtz 3
and Cal 3 display evidence of tensional opening (Sibson et al., 1975) and a syntaxial
growth with fibers perpendicular to vein wall (Fig. 3.4C).
90

Figure 3.3. Mineral paragenesis of the Beaverlodge U deposits showing regional greenschist
metamorphism during exhumation of the fault zones to shallow crustal levels subsequent to
mylonitization. Shown are six distinct stages of U mineralization that result from episodic
tectonic reactivation of fault zones at shallower crustal levels. The main event of U
mineralization occurs during the brecciation stage. The thickness of the lines indicates the
relative mineral abundance. Temperatures associated with the different alteration minerals
91

are derived from their chlorite crystal chemistry. The fluid composition is derived from the
crystal chemistry of chlorite and U and from REE abundance of uraninite. The origin of the
fluid is obtained from stable isotope geochemistry of chlorite and calcite in textural
equilibrium with the U mineralization. The age of each event of U mineralization corresponds
to the 207 Pb/ 206 Pb age obtained from LA-HR-ICPMS on uraninite (Dieng et al., 2011).
Cl=chlorite crystal chemistry, U=Uraninite crystal chemistry, SI=Stable isotope,
Pg=Paragenesis assemblage.
Granite-related metasomatic-type alteration affected the Gunnar granite (Figs. 3.4E
and 3.4F) and involved pervasive Ab 2 albite metasomatism. Replacement of Kfs 1 K-
feldspar is complete and precedes Qtz 1 quartz dissolution resulting in a rock exclusively
composed of Ab 2 albite (Fig. 3.4E), which is further carbonatized by Cal 5 . This calcite
occupies voids left after Qtz 1 quartz dissolution. Petrographic evidence shows that the U 3
mineralization was introduced subsequent to the albitization process and occupied space
between Ab 2 albite grains probably left after Cal 5 calcite and Qtz 1 quartz dissolution. U 3
uraninite is intergrown with Chl 5 chlorite, Src 3 sericite, Hem 5 hematite, Cal 6 calcite, Mz 1
monazite, and Ttn 2 titanite (Fig. 3.4F). Late alteration associated with Cal 7 calcite, Qtz 4
quartz and Chl 6 chlorite veins locally crosscut the mineralized albitized granite (Fig. 3.3).
Breccias are associated with the main U-mineralizing event throughout the
Beaverlodge area and result from a brittle reactivation of shear zones (Dieng et al., 2011).
The breccia is composed of variable-sized (3-4 cm), locally albitized cataclasite and
mylonite rock fragments, embedded in a Cal 8 calcite matrix (Fig. 3.4G). The matrix also
contains broken fragments of Qtz 1 quartz and Kfs 1 feldspar. U 4 uraninite is associated with
minor fine-grained (

fragments or as dissemination in the Cal 8 calcite matrix associated with Chl 7 chlorite
(Figs. 3.4G and 3.4H).
93

Figure 3.4. Photomicrographs of typical mineral assemblages and crosscutting relationship in
the Beaverlodge area illustrating the mineral paragenesis in Figure 3: A: Transmitted light
photomicrograph of a cataclasite granite gneiss with mylonitized fragments, Qtz 1 and Kfs 1
embedded in a matrix of ±U 1 , Cal 2 , Hem 3 , Chl 3 , Src 2 , Cpy 2 , and Py 2 . B: Reflected light
photomicrograph showing U 1 associated with Hem 3 and Py 2 . C: Transmitted light
photomicrograph of U 2 -Hem 4 -Chl 4 -Cal 4 -Cpy 3 -Py 3 vein cutting cataclasite rock and filled by
94

tensional mode I vein of Qtz 3 and Cal 3 . D: Reflected light photomicrograph of U 2 replacing
Py 3 in vein. E: Transmitted light photomicrograph of mineralized albite-metasomatized
granite showing U 3 associated with Hem 5 and Ttn 2 in void left after Cal 5 and Qtz 1 dissolution.
F: Reflected light photomicrograph of mineralized albite-metasomatized granite. G:
Transmitted light photomicrograph of mineralized breccia with albitized fragments of
cataclasite rock in Cal 8 matrix. U 4 rims breccia fragments and disseminated in Cal 8 matrix
associated with Chl 7 , and Hem 6 . H: Reflected light photomicrograph of a highly U-
mineralized breccia. U 4 with Cal 8 and Chl 7 forming the matrix. I: Transmitted light
photomicrograph of breccia vein composed of crushed Qtz 1 , Kfs 1 and Cal 1 embedded in a
chlorite-rich matrix. U 5 is disseminated in the matrix associated with Hem 7 , Chl 8 and Ap 1 . J:
Reflected light photomicrograph of breccia vein. K: Transmitted light photomicrograph of
late mineralized veins containing U 6 , Chl 9 and Hem 8 . L: Reflected light photomicrograph of
the late mineralized veins.
Locally, U 4 uraninite displays a colloform texture with concentric banding indicating
effects of late fluid alteration events. Chl 7 chlorite generally forms radiating aggregates
enveloping U 4 uraninite. The size and texture of Chl 7 chlorite indicate growth into open
pore spaces that were possibly created by brittle deformation. U 4 is associated with Src 3
sericite, Hem 6 hematite, Py 5 pyrite, and Cpy 4 chalcopyrite. In places, U 4 replaces Py 4
pyrite.
U 5 uranium mineralization associated with mafic dikes occurs as veinlets or
millimetric to metric breccia-dikes crosscutting the shear zone at Cinch Lake (Dieng et al.,
2011). Field observations indicate a spatial relationship between breccia-dikes and mafic
dikes. Breccia-dikes are composed of angular country rock fragments, Qtz 1 quartz, Kfs 1
feldspar and Cal 1 calcite grains embedded in a chlorite matrix (Fig. 3.4I). U 5 occurs as
disseminated grains cementing altered fragments (Fig. 3.4J) and is intergrown with Chl 8
chlorite, Cal 9 calcite, Src 4 sericite, Hem 7 hematite, Mzn 2 monazite, and Ttn 3 titanite (Fig.
95

3.4J). Py 6 Pyrite and Cpy 5 chalcopyrite are disseminated in the matrix. Ap 1 apatite as
tabular crystals is intergrown with U 5 (Fig. 3.4J).
Athabasca-type U mineralization fills late fractures and consists of U 6 uraninite
associated with Cal 10 calcite, Chl 9 chlorite, Hem 8 hematite, and minor Py 7 pyrite (Fig.
3.4L). These late veins (Fig. 3.4K) crosscut the Murmac Bay Group, the basal
conglomerates of the Martin Lake Group and the mafic dikes and are the youngest
mineralized phase. U 6 uraninite is typically massive and generally rims Cal 10 calcite veins.
Late veins of Cal 11 calcite, Chl 10 chlorite, Qtz 5 quartz and sulfide occur as fracture-filling
minerals cutting primary ore assemblages. The sulfides are Gn 1 galena, Cpy 6 chalcopyrite,
Py 8 pyrite, Sph 1 sphalerite, and copper minerals. Gn 1 galena forms inclusions or fracturefilling
in uraninite and Py 8 pyrite or thin films along Cal 8 calcite cleavage in the breccia
rock. Sph 1
sphalerite occurs as irregular masses or fine blebs in Py 8 pyrite. Copper
mineralization is present as disseminated aggregates of Bn 1 bornite, Dg 1 digenite, and Cv 1
covellite at the Ace-Fay and Gunnar deposits and appears to postdate the main event of U
mineralization.
3.4.2. Crystal Chemistry
3.4.2.1. Mineral chemistry of uraninite and brannerite
Electron microprobe and backscattered images reveal that uraninite from all stages of
mineralization has been variably altered to different forms of uranyl-silicates (Table 3.1,
Fig. 3.5). These uraninites demonstrate evidence of considerable variation in reflectance,
suggesting significant heterogeneity in their chemical composition as a result of variable
alteration by later fluids (Kotzer and Kyser, 1993; Alexandre et al., 2005).
96

Chemical Pb Age (Ma)
Figure 3.5. Content of substituting elements in uraninite as function of the chemical Pb age of
different generations of uraninite in U deposits in the Beaverlodge area. Arrow indicates the
effect of alteration by later fluids.
The most altered samples are those of the granite-related metasomatic-type U 3
uraninite from the Gunnar deposit (Fig. 3.5). In U 3 uraninite, the concentration of PbO is
the lowest and the total Ca+Fe+Si the highest, reflecting a higher degree of postmineralization
alteration that has affected U 3 uraninite subsequent to its formation. U 3
uraninite has high P 2 O 5 and Y 2 O 3 contents. In contrast, U 4 uraninite from the breccia-type
mineralization is less altered than U 3 uraninite. The concentration of UO 2 in U 4 uraninite
varies from 73.23 to 78.93 weight percent and PbO contents range from 8.71 to 19.45
weight percent (Table 3.1). The chemical composition of well-preserved breccia-type U 4
uraninite indicates elevated MnO, Y 2 O 3 , SO 3 , and ThO contents (Table 3.1). Other
elements present within the U 4 uraninite structure include CaO, SiO 2 , FeO, and TiO 2
(Table 3.1). The concentration of UO 2 in Br 1
brannerite from the breccia-type
97

mineralization varies from 25.70 to 42.40 weight percent and TiO 2 contents vary
inversely, from 52.90 to 13.36 weight percent. Br 1 brannerite contains also several weight
percent of CaO, FeO, SiO 2, PbO (Table 3.1), and anomalous levels of V 2 O 3, MnO, P 2 O 5 ,
SO 3 , ThO, and Y 2 O 3 (Table 3.1) . The presence of these elements in Br 1 brannerite is likely
a result of post-precipitation alteration involving oxidation and partial hydration of the
mineral (Smith, 1984).
Volcanic-type U 5 uraninite has high contents of MnO, V 2 O 3 , and TiO 2 (Table 3.1).
The high TiO 2 content is consistent with the presence of Ttn 3 titanite intergrown with U 5
uraninite. The concentration of UO 2 varies from 70.31 to 76.1 weight percent (Table 3.1).
The Pb contents are variable ranging from 0.85 to 20.40 weight percent. There are high
Ca, Si, and Fe contents within the U 5 uraninite structure. Athabasca-type U 6 uraninite
contains the highest concentrations of P 2 O 5 (Table 3.1). V 2 O 3 and MnO also are present in
variable amounts.
Sample ID UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Early tensional vein-type U 2 mineralization
6122_Pt21 71.83 2.02 3.61 0.39 0.40 0.02 0.11 17.88 0.02 0.03 0.02 0.05 0.12 0.00 0.14 0.03 96.50
6122_Pt22 54.29 0.64 11.73 1.29 0.39 0.04 0.16 15.31 0.01 0.00 0.04 0.04 0.10 0.03 0.06 0.01 83.99
6122_Pt31 73.07 3.05 3.44 0.91 0.38 0.05 0.03 14.52 0.04 0.09 0.01 0.02 0.15 0.07 0.11 0.07 95.90
6122_Pt4_1 37.29 0.69 39.21 0.44 0.13 0.01 0.04 7.66 0.11 0.04 0.04 0.09 0.50 0.00 0.08 0.02 86.03
6122_Pt4_2 72.61 0.59 3.33 0.31 0.65 0.02 0.04 17.42 0.03 0.02 0.02 0.03 0.18 0.04 0.02 0.00 95.29
6122_Pt5_1 71.65 0.46 2.32 0.11 0.38 0.04 0.05 19.91 0.02 0.05 0.00 0.01 0.07 0.09 0.01 0.02 95.09
6122_Pt92 78.10 1.92 3.38 0.95 2.58 0.03 0.17 7.11 0.05 0.05 0.00 0.02 0.43 0.02 0.00 0.04 94.74
6122_Pt101 73.63 9.89 2.48 1.14 1.35 0.28 0.23 1.90 0.36 0.05 0.01 0.03 0.36 0.08 0.20 0.05 91.80
Granite related metasomatic-type U 3 mineralization at the Gunnar deposit
6134pt21 77.59 3.01 5.35 0.15 0.06 0.01 0.04 0.07 0.12 0.14 0.01 0.01 0.02 0.02 0.07 0.04 86.61
6134pt22 80.25 3.04 5.60 0.22 0.03 0.01 0.09 0.12 0.00 0.08 0.03 0.00 0.08 0.04 0.06 0.04 89.46
6134pt23 78.63 3.65 5.19 1.65 0.33 0.01 0.06 0.00 0.06 0.07 0.02 0.02 0.06 0.00 0.07 0.12 89.78
6134pt24 78.36 3.72 5.28 1.82 0.44 0.05 0.02 0.03 0.06 0.06 0.05 0.02 0.05 0.01 0.05 0.02 89.84
6134pt3 77.88 4.95 5.57 0.19 0.37 0.01 0.01 0.11 0.05 0.07 0.03 0.01 0.09 0.01 0.08 0.01 89.33
6134pt31 79.27 3.95 5.52 0.15 0.01 0.03 0.04 0.11 0.08 0.08 0.04 0.01 0.03 0.00 0.04 0.02 89.22
6134pt32 81.64 3.39 4.56 0.16 0.00 0.12 0.07 0.03 0.05 0.06 0.04 0.00 0.07 0.03 0.08 0.05 90.13
6134pt33 79.50 3.78 5.54 0.11 0.06 0.04 0.02 0.06 0.09 0.06 0.02 0.00 0.04 0.00 0.06 0.01 89.23
6134pt41 80.77 3.52 5.67 0.23 0.01 0.01 0.00 0.13 0.01 0.07 0.03 0.01 0.09 0.04 0.01 0.04 90.57
6134pt42 79.52 3.13 5.90 0.26 0.13 0.01 0.03 0.09 0.07 0.05 0.00 0.03 0.07 0.00 0.03 0.01 89.31
6134pt43 81.29 2.79 5.67 0.20 0.03 0.00 0.02 0.16 0.01 0.05 0.02 0.00 0.07 0.03 0.04 0.02 90.28
6134pt51 81.39 2.70 5.41 0.13 0.00 0.04 0.00 0.11 0.04 0.06 0.07 0.00 0.04 0.06 0.02 0.07 89.88
6134pt52 74.27 3.20 4.97 0.22 0.08 0.04 0.02 0.04 0.11 0.23 0.02 0.01 0.10 0.02 0.05 0.04 83.27
98

6134pt53 80.12 4.95 4.53 0.22 0.41 0.01 0.01 0.10 0.12 0.11 0.05 0.01 0.02 0.16 0.00 0.01 90.75
6134pt61 81.12 3.04 5.23 0.01 0.01 0.03 0.01 0.03 0.00 0.04 0.02 0.01 0.01 0.01 0.02 0.01 89.49
6134pt62 81.92 3.06 5.24 0.04 0.04 0.00 0.00 0.10 0.01 0.04 0.02 0.00 0.08 0.04 0.04 0.04 90.45
6134pt63 80.49 3.09 5.36 0.01 0.02 0.01 0.09 0.08 0.04 0.06 0.01 0.01 0.01 0.04 0.09 0.01 89.37
6134pt64 81.96 3.12 4.98 0.05 0.04 0.01 0.02 0.10 0.02 0.06 0.04 0.00 0.07 0.02 0.01 0.01 90.44
6134pt81 79.17 2.87 4.43 0.01 0.02 0.01 0.56 1.40 0.09 0.07 0.02 0.10 0.03 0.16 0.07 0.01 88.96
6134pt82 79.67 2.90 4.69 0.02 0.07 0.03 0.35 1.44 0.06 0.00 0.03 0.07 0.02 0.08 0.10 0.05 89.42
6134pt83 80.29 3.14 3.87 0.03 0.78 0.01 0.05 0.11 0.08 0.03 0.04 0.00 0.04 0.12 0.00 0.00 88.53
6134pt84 77.08 2.76 5.44 0.04 0.02 0.02 0.52 0.61 0.09 0.01 0.00 0.04 0.06 0.21 0.02 0.04 86.86
6134pt8a1 80.50 4.02 5.50 0.04 0.11 0.02 0.00 0.07 0.01 0.12 0.06 0.02 0.07 0.05 0.03 0.00 90.45
6134pt8a2 82.92 2.92 5.30 0.07 0.04 0.02 0.09 0.11 0.01 0.07 0.01 0.04 0.09 0.01 0.07 0.02 91.62
6134pt8a3 77.51 1.83 5.81 0.17 0.02 0.02 0.05 0.16 0.11 0.15 0.00 0.03 0.12 0.01 0.05 0.06 85.99
6134pt91 63.41 3.15 4.32 0.08 0.04 0.03 0.24 1.46 0.18 0.19 0.03 0.05 0.08 0.12 0.05 0.02 73.42
6134pt92 75.28 3.78 5.33 0.02 0.07 0.01 0.29 1.41 0.22 0.08 0.00 0.03 0.01 0.20 0.02 0.07 86.69
6134pt93 73.41 2.98 5.18 0.09 0.09 0.05 0.31 1.60 0.28 0.29 0.03 0.02 0.07 0.19 0.06 0.03 84.62
6134pt9a1 81.55 3.36 4.25 0.18 0.69 0.00 0.08 0.07 0.15 0.10 0.01 0.01 0.06 0.07 0.02 0.00 90.57
6134pt9a2 80.44 2.93 4.23 0.04 0.47 0.06 0.14 0.20 0.15 0.07 0.01 0.01 0.05 0.13 0.02 0.04 88.96
6134pt9a3 78.82 3.02 4.69 0.02 0.60 0.03 0.15 0.05 0.14 0.05 0.01 0.00 0.03 0.15 0.04 0.05 87.79
6134pt9a4 77.24 5.45 4.77 0.44 0.46 0.04 0.00 0.12 0.19 0.16 0.00 0.01 0.09 0.16 0.05 0.03 89.07
6134pt101 73.83 6.55 3.47 1.32 0.00 0.03 0.07 0.41 0.09 0.14 0.00 0.01 0.05 0.27 0.01 0.06 86.09
6134pt102 64.50 9.49 2.43 9.15 0.06 0.01 0.12 0.65 0.12 0.28 0.06 0.03 0.05 0.32 0.26 0.05 87.17
6134pt103 74.14 7.47 3.23 1.59 0.01 0.01 0.06 0.32 0.04 0.16 0.00 0.01 0.01 0.27 0.03 0.04 87.34
6134pt104 74.03 5.88 2.71 1.97 0.08 0.01 0.18 1.96 0.14 0.13 0.03 0.01 0.01 0.41 0.03 0.07 87.58
6134pt105 72.59 6.19 3.29 2.40 0.04 0.02 0.08 1.39 0.14 0.15 0.02 0.01 0.03 0.26 0.11 0.01 86.58
Breccia-type U 4 mineralization
Uraninite
VRB_pt41 74.17 0.45 2.70 0.76 0.41 0.01 0.18 19.22 0.00 0.05 0.08 0.02 0.14 0.13 0.03 0.05 98.29
5812Pt21 73.23 0.47 3.24 0.53 0.43 0.04 0.04 18.45 0.01 0.02 0.14 0.01 0.16 0.16 0.04 0.01 96.91
5812Pt61 74.88 0.54 4.43 0.44 0.44 0.01 0.16 15.88 0.02 0.03 0.02 0.01 0.22 0.15 0.04 0.00 97.16
5812Pt11 75.58 0.50 4.51 0.62 0.46 0.03 0.18 12.07 0.02 0.04 0.03 0.01 0.42 0.45 0.08 0.05 94.92
5812Pt82 78.94 0.69 4.43 0.99 0.55 0.06 0.08 9.52 0.01 0.03 0.17 0.01 0.27 0.08 0.06 0.02 95.72
5812Pt12 76.71 0.98 6.43 0.90 0.61 0.03 0.21 6.89 0.01 0.03 0.04 0.06 0.70 0.60 0.00 0.01 94.18
5812Pt81 77.99 1.05 4.27 1.20 0.80 0.05 0.01 8.71 0.02 0.03 0.29 0.03 0.35 0.06 0.05 0.02 94.82
5812Pt22 75.02 2.40 4.63 1.28 1.74 0.01 0.14 10.07 0.05 0.05 0.03 0.73 0.67 0.31 0.11 0.03 97.15
Brannerite
5812Pt41 42.40 14.29 1.51 2.09 13.36 0.02 0.18 12.43 0.55 0.07 0.56 2.15 0.04 0.14 0.08 0.08 89.88
5812Pt31 27.03 4.83 19.26 3.17 26.60 0.11 0.20 0.81 0.03 0.05 0.04 0.01 0.17 0.01 0.08 0.04 82.29
5812Pt71 36.98 8.11 2.27 2.98 34.85 0.16 0.64 2.89 0.03 0.05 0.10 0.23 0.27 0.03 0.05 0.05 89.61
5812Pt42 34.57 3.88 9.83 2.11 36.31 0.23 0.35 1.47 0.02 0.01 0.13 0.01 0.32 0.01 0.01 0.01 89.25
5812Pt51 37.19 5.75 2.29 2.64 41.70 0.14 0.41 1.87 0.02 0.01 0.11 0.15 0.16 0.02 0.01 0.04 92.48
5812Pt72 34.34 5.10 2.06 3.13 44.54 0.13 0.46 1.91 0.01 0.02 0.06 0.09 0.23 0.01 0.11 0.04 92.09
5812Pt52 32.87 4.46 2.05 3.10 47.65 0.17 0.37 1.74 0.02 0.00 0.13 0.10 0.17 0.00 0.04 0.01 92.84
5812Pt32 25.70 4.77 4.33 4.16 52.90 0.18 0.26 1.42 0.01 0.03 0.09 0.05 0.15 0.01 0.09 0.01 94.04
Volcanic-type U 5 mineralization
6120B_pt1 76.10 0.89 3.71 0.62 0.58 0.03 0.16 13.77 0.00 0.03 0.04 0.02 0.22 0.01 0.04 0.05 96.13
6120B_pt12 73.42 1.05 2.73 0.45 0.52 0.01 0.48 17.56 0.06 0.03 0.07 0.04 0.12 0.01 0.03 0.07 96.46
6120B_pt22 71.88 1.43 3.00 0.46 0.48 0.03 0.25 17.14 0.06 0.02 0.00 0.01 0.08 0.01 0.07 0.03 94.86
6120B_pt31 74.41 0.84 3.66 0.48 0.64 0.01 0.22 15.41 0.06 0.03 0.02 0.02 0.20 0.03 0.09 0.03 95.99
6120B_pt32 74.38 1.68 2.57 0.54 0.58 0.03 0.13 15.68 0.03 0.03 0.00 0.02 0.10 0.09 0.00 0.03 95.82
6120B_pt33 73.75 0.47 3.05 0.28 0.42 0.03 0.09 17.91 0.05 0.04 0.05 0.00 0.07 0.03 0.06 0.04 96.19
6120B_pt34 74.03 0.50 2.50 0.32 0.30 0.03 0.13 20.15 0.04 0.03 0.02 0.03 0.00 0.02 0.03 0.04 98.05
6120B_pt41 71.92 0.51 2.33 0.05 0.51 0.01 0.11 20.29 0.03 0.02 0.08 0.04 0.04 0.09 0.06 0.02 95.99
6120B_pt35 74.17 9.32 1.73 2.09 1.11 0.02 0.22 0.85 0.07 0.05 0.04 0.01 0.23 0.00 0.03 0.00 89.82
6120B_pt36 74.44 9.51 1.67 1.36 1.14 0.05 0.23 1.78 0.07 0.03 0.02 0.29 0.20 0.01 0.05 0.02 90.72
6120B_pt41 70.14 0.67 2.65 0.15 0.37 0.01 0.33 19.62 0.04 0.02 0.05 0.02 0.08 0.04 0.08 0.01 94.13
6120B_pt42 74.34 1.12 4.30 0.95 0.43 0.02 0.26 14.17 0.05 0.03 0.01 0.01 0.23 0.04 0.02 0.00 95.92
6120B_pt51 72.87 0.38 2.37 0.23 0.29 0.01 0.16 19.91 0.05 0.02 0.01 0.04 0.04 0.11 0.09 0.03 96.56
6120B_pt52 73.23 0.46 2.58 0.43 0.36 0.03 0.04 19.04 0.03 0.03 0.01 0.01 0.07 0.06 0.03 0.03 96.37
6120B_pt61 71.72 0.92 2.35 0.28 0.49 0.04 0.46 19.28 0.04 0.02 0.02 0.03 0.01 0.03 0.05 0.01 95.67
6120B_pt62 70.31 0.64 2.65 0.39 0.40 0.05 0.22 20.24 0.07 0.01 0.06 0.04 0.06 0.06 0.04 0.02 95.15
Athabasca-type U 6 mineralization
6137APt42 63.93 6.67 12.03 2.91 0.04 0.01 0.17 0.67 0.07 0.01 0.03 0.03 0.54 0.00 0.06 0.05 87.13
6137APt51 35.55 9.15 24.28 7.30 0.00 0.03 0.10 0.80 0.04 0.05 0.02 0.01 0.47 0.00 0.12 0.03 77.73
6137APt52 24.60 20.95 1.53 22.12 0.02 0.00 0.22 0.31 0.01 0.01 0.01 0.00 0.35 0.00 0.53 0.00 70.12
6137APt61 61.82 4.25 16.19 2.40 0.08 0.01 0.20 2.04 0.04 0.05 0.03 0.03 0.57 0.01 0.03 0.03 87.68
99

6137APt71 60.67 13.73 4.59 6.48 0.05 0.01 0.23 0.48 0.03 0.04 0.02 0.00 0.53 0.01 0.18 0.01 86.84
6137APt72 48.70 10.57 6.69 9.26 0.04 0.01 0.03 0.54 0.05 0.08 0.03 0.02 0.45 0.02 0.25 0.02 76.46
6137APt81 26.87 21.78 13.43 4.68 0.05 0.31 0.21 0.24 0.07 0.15 0.02 0.00 0.30 0.07 0.17 0.02 68.18
6137APt82 60.21 16.36 3.11 4.97 0.11 0.04 0.13 0.17 0.16 0.14 0.02 0.00 0.51 0.08 0.02 0.04 86.00
6137APt9 60.59 9.42 13.24 2.45 0.15 0.03 0.37 0.97 0.83 0.02 0.04 0.02 0.47 0.42 0.03 0.01 88.98
Table 3.1. Electron microprobe analysis and chemical composition of uraninite and
brannerite from different generations of U mineralization in the Beaverlodge area.
3.4.2.2. Chlorite Crystal Chemistry
Chlorite is associated with all stages of U mineralization and is used here to estimate
temperatures and compositions of the mineralizing fluids. The chemical formulas and
formation temperatures of chlorite from different types of U mineralization are
summarized in Table 3.2.
Average Structural Formulae of various generations of Chlorites
Temperature of
Formation ( o C)
1 Mg 3.185Fe 1.72Al 1.Ca 0.02 (Si 3.19Al 0.81) O 10 (F 0.15 (OH) 7.85) 200
2 Mg 2.62Fe 1.22Al 2.66Ca 0.4 (Si 2.85Al 1.16) O 10 (F 0.14CL 0.02 (OH) 7.84) 310
3.a Mg 2.86Fe 1.82Al 2.41Ca 0.02Mn 0.03Ti 0.01 (Si 2.83Al 1.17) O 10 (F 0.09 (OH) 7.91) 315
3.b Mg 3.37Fe 1.27Al 2.29 (Si 2.94Al 1.06) O 10 (F 0.11 (OH) 7.89) 278
3.c Mg 3.34Fe 1.47Al 2.03 (Si 3.06Al 0.94) O 10 (F 0.16 (OH) 7.84) 242
3.c Mg 3.22Fe 1.64Al 1.96 (Si 3.09Al 0.91) O 10 (F 0.1 (OH) 7.90) 230
3.c Mg 3.09Fe 0.39Al 2.32 (Si 3.45Al 0.55) O 10 (F 0.43CL 0.02 (OH) 7.56) 116
4 Mg 2.06Fe 2.37Al 2.57Ca 0.1 (Si 2.79Al 1.21) O 10 (F 0.06 (OH) 7.94) 330
4.a Mg 3.71Fe 1.04Al 1.87 (Si 3.21Al 0.79) O 10 (F 0.17 (OH) 7.83) 194
5a Mg 2.40Fe 2.32Al 2.38Mn 0.03Ti 0.01 (Si 2.83Al 1.17) O 10 (F 0.04 (OH) 7.96) 320
5.b Mg 2.77Fe 2.06Al 1.95Mn 0.02 (Si 3.10Al 0.90) O 10 (F 0.02 (OH) 7.98) 229
5.b Mg 2.49Fe 2.12Al 2.29Ca 0.03Mn 0.02 (Si 3.08Al 0.92) O 10 (OH) 8 212
6 Mg 2.49Fe 2.36Al 1.97Ca 0.01 (Si 3.08Al 0.92) O 10 (F 0.13 Cl 0.01(OH) 7.86) 235
Table 3.2. Temperatures of formation, and average structural formulas of different
generations of chlorite phases from U deposits in the Beaverlodge area. Calculated
temperatures are accurate to within 25-30°C based on replicate analyses.
100

Textural evidence suggests that retrograde Chl 1
chlorite predominantly replaced
earlier metamorphic Bt 1 biotite and Hbl 1 amphibole in altered metasedimentary and
feldspar-amphibole rocks at Cinch Lake (Dieng et al., 2011). Chl 1 chlorite has high Mg
and Fe contents (19.45 and 19.74 wt. % respectively, Table 3.3), which supports
inheritance of the chemistry of Bt 1 biotite into the Chl 1 chlorite. Chl 1 chlorites have a
composition typical of Fe-clinochlore with a calculated formation temperature of ca.
200°C (Table 3.3). They have high SiO 2 contents (30.25 wt. %), uniform Fe/Al and Mg/Al
ratios and an average Fe/(Mg + Fe) ratio of 0.36, similar to the composition of retrograde
metamorphic chlorite reported by Tortosa (1983) at the Cenex mine. The chemical
composition of Chl 1 chlorite indicates that the fluid from which it formed contained Ca
and F (Table 3.3).
Chl 4 chlorite in early tensional vein-type U 2 mineralization has high Mg contents
(17.03 wt.%) and the lowest Fe contents (14.17 wt.%). These chlorites have the lowest but
relatively uniform Fe/Al, Mg/Al and Fe/Mg ratios and a calculated formation temperature
of ca. 310°C (Table 3.3). Chl 4 chlorites are Ca-F-rich and have an average Fe/(Mg+Fe)
ratio of 0.32 that is indistinguishable from retrograde Chl 1 chlorite.
Syn-ore Chl 5 chlorite in granite-related metasomatic-type U 3 at the Gunnar deposit
has high Mg and Al contents (18.17 wt.% and 19.41 wt.%, respectively) and low Fe
contents (20.58 wt.%, Table 3.3, Fig. 3.6C) with a calculated formation temperature of ca.
315°C. They have relatively uniform Fe/Al, Mg/Fe, and Mg/Al ratios and their low Fe/(Fe
+ Mg) ratios (0.37 to 0.43) attest to the Mg-rich and Fe-poor composition of the fluid.
Fluids in equilibrium with Chl 5 chlorite were relatively enriched in Ca, and F (Table 3.3;
101

Fig. 3.6A). The Ca may result from the dissolution of Cal 5 calcite. Ttn 2 titanite and Mzn 1
monazite are intergrown with Chl 5 chlorite and U 3 uraninite in the ore assemblage and are
therefore coeval. Syn-ore Chl 5 chlorite was subsequently altered by later fluids resulting in
local Mg-enrichment and Fe-depletion that form a mosaic texture. Calculated average
formation temperatures of altered Chl 5 chlorites range from 115 o C to 240 o C (Table 3.4).
Later Chl 6 chlorite veins crosscut the mineralized granite and have higher Mg and lower
Fe contents and formation temperatures of ca. 275 o (Table 3.4).
A) B)
Ti
Early vein-type
Cl
Ca
C)
D)
Figure 3.6. Ternary and binary diagrams showing the compositional variation of chlorite
phases (in wt %) from different types of U mineralization in the Beaverlodge area.
102

Syn-ore Chl 7 chlorite in breccia-type U 4 mineralization yields the relatively highest
Fe contents of 25.78 weight percent (Table 3.3; Fig. 3.6C) and high Fe/(Fe+Mg) ratios of
0.53, indicating that the U-bearing fluid was Fe-rich. The average Fe/(Mg+Fe) ratio is
similar to values reported by Tortosa (1983) for Fe-chlorite associated with the
mineralized zone at the Cenex mine. Chl 7 chlorite has a composition typical for chamosite
corresponding to formation temperatures near 330°C (Table 3.3). Cal 8 calcite and U 4
uraninite intergrowths with Chl 7 chlorite in conjunction with high F contents in Chl 7
chlorite, suggest that the U-bearing fluid contained Ca and F (Table 3.3; Figs..3.6A and
3.6B). Electron microprobe and backscattered images show that Chl 7 chlorite was
subsequently altered by fluids that were Mg-rich. These altered chlorites have average
formation temperatures near 195 o C (Table 3.4).
Syn-ore Chl 8 chlorite in volcanic-type U 5 mineralization is an Mg-Fe-chlorite with a
formation temperature of ca. 320°C (Table 3.3). Chl 8 chlorite has the highest Mn and Ti
contents (Table 3.3; Figs. 3.6A and 3.6B), although the presence of Ti and Ca reflects Ttn 3
titanite and Ap 1 apatite grains respectively, intergrown with Chl 8 chlorite and U 5 uraninite
(Fig. 3.4I). Chl 8 chlorites were subsequently altered by later Mg-rich fluids, resulting in
altered chlorites with formation temperatures near 210 o C (Table 3.4). Chl 9
chlorite
associated with the Athabasca-type U 6 mineralization has high Mg and Fe contents (15.43
wt.% and 26.01 wt.%, respectively) and is typically F-Cl-rich (Table 3.3; Figs. 3.6A and
3.6B), with formation temperatures of ca. 235°C (Table 3.3). The Fe/(Fe+Mg) ratio of
Chl 9 chlorite ranges from 0.56 to 0.67 and indicates that the U-mineralizing fluid was
likely Mg-rich.
103

Sample ID 1 ± 2 ± 3.a ± 4 ± 5.a ± 5.a ± 5.a ± 6 ±
n= 5 5 5 15 8 9 8 10
Oxides (Wt %)
SiO2 30.25 0.66 27.56 2.23 26.84 0.31 25.34 1.21 26.07 0.46 26.66 0.39 26.10 0.48 28.38 0.92
TiO2 0.00 - 0.00 - 0.06 0.02 0.02 - 0.02 - 0.01 - 0.09 0.03 0.02 -
AL2O3 14.85 0.94 21.94 3.15 19.41 0.29 19.88 1.44 18.41 0.48 19.12 0.81 18.79 0.47 15.40 0.47
CR2O3 0.02 - 0.05 - 0.00 - 0.10 - 0.02 - 0.03 - 0.01 - 0.17 0.07
FeO 19.45 0.49 14.17 1.94 20.58 0.34 25.78 4.82 28.50 0.95 23.05 2.90 25.65 0.68 26.01 3.08
MnO 0.11 0.03 0.15 0.07 0.38 0.06 0.08 0.07 0.22 0.17 0.51 0.14 0.24 0.05 0.01 -
MgO 19.74 0.85 17.03 2.56 18.17 0.38 12.60 2.26 13.18 0.63 16.60 1.39 15.13 0.30 15.43 2.05
CaO 0.15 0.09 3.47 5.00 0.01 - 0.85 1.12 0.01 - 0.02 - 0.02 - 0.08 -
NA2O 0.01 - 0.28 0.17 0.02 - 0.04 - 0.01 - 0.02 - 0.03 - 0.05 -
K2O 0.01 - 0.31 0.35 0.01 - 0.01 - 0.03 - 0.01 - 0.03 - 0.01 -
F 0.45 0.11 0.40 0.36 0.26 0.06 0.17 0.10 0.08 0.05 0.10 0.08 0.18 0.06 0.38 0.20
CL 0.00 - 0.13 0.05 0.00 - 0.01 - 0.00 - 0.00 - 0.01 - 0.04 -
H2O 11.16 0.18 11.39 11.25 0.12 10.89 0.44 10.97 0.14 11.23 0.14 11.03 0.03 10.87 0.27
O=F -0.19 - -0.17 - -0.11 - -0.02 - -0.03 - -0.04 - -0.07 - -0.16 -
O=CL 0.00 - -0.03 - 0.00 - -0.01 - 0.00 - 0.00 - 0.00 - -0.01 -
Total 96.01 1.35 97.08 3.21 96.88 0.91 95.66 5.07 97.48 0.95 97.31 0.64 97.22 0.51 96.94 1.95
Atomic proportion
Number of O 28 28 28 28 28 28 28 28
Tetrahedral sites
Si 4+ 3.19 0.04 2.85 0.06 2.83 0.02 2.79 0.05 2.84 0.03 2.83 0.02 2.81 0.05 3.08 0.08
AL 4+ 0.81 0.04 1.16 0.06 1.17 0.02 1.21 0.05 1.16 0.03 1.17 0.02 1.19 0.05 0.92 0.08
Total 4.00 4.00 4.00 4.00 4.00 4.00 4.00 4.00
Octahedral sites
AL 6+ 1.85 0.11 2.66 0.24 2.41 0.04 2.57 0.08 2.36 0.05 2.40 0.09 2.39 0.06 1.97 0.06
Ti 4+ 0.00 - 0.00 - 0.01 - 0.00 - 0.00 - 0.00 - 0.01 - 0.00 -
Cr 3+ 0.00 - 0.00 - 0.00 - 0.01 - 0.00 - 0.00 - 0.00 - 0.01 -
Fe 2+ 1.72 0.06 1.22 0.21 1.82 0.03 2.37 0.42 2.60 0.11 2.05 0.29 2.31 0.06 2.36 0.31
Mn 2+ 0.01 - 0.01 - 0.03 0.00 0.01 - 0.02 - 0.05 - 0.02 - 0.00 -
Mg 2+ 3.10 0.10 2.62 0.29 2.86 0.05 2.06 0.35 2.14 0.08 2.63 0.01 2.43 0.05 2.49 0.30
Total 6.68 0.04 6.52 0.57 7.12 0.03 7.03 0.16 7.13 0.05 7.13 0.04 7.16 0.07 6.84 0.15
Interlayers sites
Ca 2+ 0.02 - 0.40 0.59 0.00 - 0.10 0.13 0.00 - 0.00 - 0.00 - 0.01 -
Na + 0.00 - 0.06 0.04 0.00 - 0.02 - 0.00 - 0.00 - 0.01 - 0.01 -
K + 0.00 - 0.04 0.04 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 -
Total 0.02 - 0.50 0.66 0.01 - 0.12 0.07 0.01 - 0.01 - 0.01 - 0.02
Anions
F - 0.15 0.04 0.14 0.12 0.09 0.02 0.06 0.03 0.03 0.02 0.03 0.03 0.06 0.02 0.13 0.07
CL - 0.00 - 0.02 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.01 -
H + 7.85 0.04 7.84 0.12 7.91 0.02 7.94 0.05 7.97 0.02 7.97 0.03 7.94 0.02 7.86 0.07
Total 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00
O 2- 17.85 0.04 17.84 0.12 17.92 0.02 17.98 0.05 17.97 0.02 17.97 0.03 17.94 0.02 17.86 0.07
∑Cat 9.89 0.02 9.87 0.19 9.96 0.02 9.93 0.05 9.98 0.02 9.97 0.04 9.99 0.02 9.94 0.07
∑ions 18.00 0.00 18.00 0.00 18.00 0.02 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00
Temperatures ( o C)
200 14 310 20 315 6 330 16 311 9 313 7 338 16 235 24
Table 3.3. Representative electron microprobe analysis of different generations of syn-ore
chlorite phases from U deposits in the Beaverlodge area, including formation temperatures
calculated using the method of Cathelineau (1988). 1=Retrograde metamorphic Chl 1 ; 2=Chl 4
in early tensional vein type U 2 mineralization; 3a=Chl 5 in metasomatic-type U 3
mineralization at Gunnar; 4=Chl 7 in breccia-type main U 4
mineralization; 5a=Chl 8 in
volcanic-type U 5 mineralization; 6=Chl 9 in Athabasca-type U 5 mineralization. One sigma
variations are also shown. Paragenesis of all phases analyzed is shown in Figures 3 and 4 (see
the text for more details). n= number of analyses
104

Sample ID 3.b ± 3.c ± 3.d ± 3.e ± 4.a ± 5.b ± 5.c ±
n= 5 13 5 4 6 8 6
Oxides (Wt %)
SiO2 29.15 0.39 29.48 1.16 29.54 0.39 35.50 0.77 31.27 1.03 29.27 0.98 30.16 1.19
TiO2 0.01 - 0.02 - 0.01 - 0.01 - 0.03 - 0.02 - 0.02 -
AL2O3 19.28 0.26 16.65 1.08 15.90 0.26 20.27 1.21 15.46 1.21 15.65 1.27 17.88 0.27
CR2O3 0.06 - 0.02 - 0.03 - 0.01 - 0.00 - 0.05 - 0.04 -
FeO 15.02 1.17 16.95 3.65 18.76 1.17 4.79 2.61 12.13 1.91 23.28 3.21 23.31 0.97
MnO 0.24 0.07 0.20 - 0.05 0.02 0.26 0.07 0.16 0.06 0.26 0.08 0.19 0.06
MgO 22.38 1.27 21.74 3.76 20.61 0.32 21.33 0.90 24.25 1.31 17.56 1.79 10.79 0.71
CaO 0.03 0.01 0.03 0.03 0.01 1.03 0.62 0.14 0.05 0.11 0.08 0.30 0.05
NA2O 0.01 - 0.04 0.04 0.01 - 0.05 - 0.02 - 0.05 - 0.19 -
K2O 0.01 - 0.02 - 0.02 - 0.17 - 0.01 - 0.02 - 1.09 -
F 0.36 0.05 0.48 0.25 0.31 0.06 1.38 0.57 0.51 0.12 0.28 0.09 0.00 -
CL 0.00 - 0.00 - 0.00 - 0.11 0.04 0.00 - 0.00 - 0.00 -
H2O 11.71 0.09 11.39 0.29 11.31 0.11 11.67 0.32 11.45 0.24 11.30 0.23 11.05 0.11
O=F -0.15 - -0.20 - -0.13 - -0.59 - -0.22 - -0.03 - 0.00 -
O=CL 0.00 - 0.00 - 0.00 - -0.02 - 0.00 - 0.00 - 0.00 -
Total 98.10 0.41 96.99 1.30 96.44 0.73 96.04 1.51 95.21 1.90 97.61 2.10 95.01 0.36
Atomic proportion
Number of O 28 28 28 28 28 28 28
Tetrahedral sites
Si 4+ 2.94 0.02 3.06 0.06 3.09 0.03 3.45 0.08 3.21 0.07 3.10 0.08 3.27 0.10
AL 4+ 1.06 0.02 0.94 0.06 0.91 0.03 0.55 0.08 0.79 0.07 0.90 0.08 0.73 0.10
Total 4.00 4.00 4.00 4.00 4.00 4.00 4.00
Octahedral sites
AL 6+ 2.29 0.05 2.03 0.17 1.96 0.02 2.32 0.10 1.87 0.09 1.95 0.14 2.29 0.02
Ti 4+ 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 -
Cr 3+ 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 - 0.00 -
Fe 2+ 1.27 0.11 1.47 0.35 1.64 0.08 0.39 0.21 1.04 0.17 2.06 0.31 2.12 0.11
Mn 2+ 0.02 0.01 0.02 0.02 0.00 - 0.02 - 0.01 - 0.02 - 0.02 -
Mg 2+ 3.37 0.18 3.34 0.51 3.22 0.04 3.09 0.17 3.71 0.16 2.77 0.30 1.75 0.13
Total 6.96 6.85 0.05 6.83 0.05 5.82 0.19 6.63 0.10 6.81 0.13 6.18 0.22
Interlayers sites
Ca 2+ 0.00 - 0.00 - 0.00 - 0.11 0.07 0.02 - 0.01 - 0.03 0.01
Na + 0.00 - 0.01 - 0.00 - 0.01 - 0.00 - 0.01 - 0.04 -
K + 0.00 - 0.00 - 0.00 - 0.02 - 0.00 - 0.00 - 0.15 -
Total 0.01 - 0.01 - 0.01 - 0.14 0.07 0.02 - 0.02 - 0.22 0.06
Anions
F - 0.11 0.02 0.16 0.08 0.10 0.02 0.43 0.18 0.17 0.04 0.02 - 0.00 -
CL - 0.00 - 0.00 - 0.00 - 0.02 - 0.00 - 0.00 - 0.00 -
H + 7.89 0.02 7.84 0.08 7.90 0.02 7.56 0.18 7.83 0.04 7.98 0.06 8.00 0.06
Total 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00 8.00 0.00
O 2- 17.89 0.02 17.84 0.08 17.90 0.02 17.56 0.18 17.83 0.04 17.98 0.06 18.00 0.00
∑Cat 9.91 0.03 9.93 0.05 9.93 0.03 9.41 0.08 9.86 0.03 9.93 0.07 9.68 0.08
∑ions 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00 18.00 0.00
Temperatures ( o C)
278 7 242 20 230 8 116 24 194 23 229 25 212 32
Table 3.4. Representative electron microprobe analysis of various chlorites affected by late
low-temperature alteration phases from U deposits in the Beaverlodge area, including
formation temperatures (Cathelineau, 1988). 3a, 3b, 3c, 3d=altered Chl 5 in metasomatic-type
U 3 mineralization at Gunnar; 4a=altered Chl 7 in breccia-type U 4 mineralization; 5b,
5c=altered Chl 8 in volcanic-type U 5 mineralization. n= number of analyses
3.4.3. Isotopic compositions of minerals and fluids involved in the U mineralization
3.4.3.1. Oxygen and carbon isotopes of Calcite
105

Stable isotopic O and C compositions were determined for calcite in textural
equilibrium with uraninite for each of the U mineralization events in the Beaverlodge area
(Fig. 3.7; Table 3.5).
Figure 3.7. Calculated δ 18 O and δ 13 C values of mineralizing fluids in equilibrium with
carbonate minerals. (Legend as in Fig. 3.8)
Syn-ore Cal 6 calcite in the granite-related metasomatic-type U 3 at the Gunnar
deposit has a wide range of δ 18 O values from 7.5 per mil to 22.6 per mil, but a narrow
range of δ 13 C values comprising between -4.9 per mil and -3.4 per mil (Fig. 3.7; Table
3.5). Using a formation temperature of 315°C based on coeval Chl 5 chlorite, Cal 6 calcite
precipitated from a CO 2 -bearing fluid having δ 18 O fluid and δ 13 C fluid values between 2.5 per
mil and 17.6 per mil, and -7.1 per mil and -5.5 per mil, respectively (Fig. 3.7; Table 3.5).
Syn-ore Cal 4 calcite in the early tensional vein-type U 2 mineralization has δ 18 O values
106

anging between 15.5 per mil and 24.1 per mil and δ 13 C values ranging from -2.4 per mil
to -2.1 per mil (Fig. 3.7; Table 3.5). Assuming a formation temperature of 300°C based on
coeval Chl 4 chlorite (Table 3.3), Cal 4 formed from fluids with δ 18 O fluid values varying
between 10.2 and 18.8 per mil and δ 13 C fluid values between -4.6 per mil and -4.2 per mil
(Fig. 3.7; Table 3.5).
Sample ID Deposit Mineral
Mineral values Temperatures Fluid values
δ 18 O
V-SMOW
per mil
δ 13 C
V-PDB
per mil
o C
δ 18 O fluid
V-SMOW
per mil
δ 13 C fluid
V-PDB
per mil
Metasomatic-type U 3 mineralization
6134 Gunnar Dolomite-Calcite 22.6 -4.9 315 17.6 -7
6134D Gunnar Dolomite-Calcite 22.5 -4.9 315 17.5 -7.1
GN-03 Gunnar Calcite 7.5 -3.9 315 2.5 -6
GN-03D Gunnar Calcite 7.6 -3.8 315 2.6 -5.9
VR-190 Gunnar Calcite 12.5 -3.4 315 7.5 -5.5
VR-190D Gunnar Calcite 12.6 -3.4 315 7.6 -5.6
Early tensional vein-type U 2 mineralization
6120 Ace-Fay MG-Calcite 15.5 -2.2 310 10.2 -4.3
6120 DUP Ace-Fay MG-Calcite 15.6 -2.1 310 10.3 -4.2
6120D Ace-Fay MG-Calcite 15.5 -2.2 310 10.3 -4.3
C-22-111 Cinch Lake Dolomite-Calcite 21.3 -2.2 310 16 -4.3
C-22-93 Cinch Lake Dolomite 24.1 -2.4 310 18.8 -4.5
M51-5996-VEIN Cinch Lake Dolomite 16.9 -2.5 310 11.7 -4.6
Breccia-type U 4 mineralization
5799 Ace-Fay Calcite 10.9 -2.4 330 6.2 -4.9
5810 Ace-Fay Calcite 10.8 -4.5 330 6 -6.9
5812 Ace-Fay Dolomite-Calcite 12.1 -2.5 330 7.3 -4.9
5812D Ace-Fay Dolomite-Calcite 12.2 -2.3 330 7.4 -4.8
5812-1 Ace-Fay Dolomite 11.9 -1.6 330 7.1 -4
5800A Ace-Fay Dolomite-Calcite 12.3 -2.9 330 7.6 -5.3
5800B Ace-Fay Dolomite-Calcite 12.2 -2.9 330 7.5 -5.4
C-16-285 Cinch Lake MG-Calcite 10.6 -2.2 330 5.9 -4.6
C-22-128 Cinch Lake Calcite 13.3 -2.6 330 8.5 -5
C-22-128D Cinch Lake Calcite 13.3 -2.3 330 8.5 -4.8
C-27-198 Cinch Lake Calcite 13.3 -1.8 330 8.5 -4.2
C-27-200 Cinch Lake MG-Calcite 10.6 -2.5 330 5.9 -4.9
C-27-200D Cinch Lake Calcite 10.9 -2.4 330 6.1 -4.8
C-27-373 Cinch Lake Calcite 9.8 -2.2 330 5.1 -4.6
C-27-379 Cinch Lake Calcite 12.3 -3.8 330 7.6 -6.2
C-42-167 Cinch Lake MG-Calcite 12 -2.6 330 7.2 -5
C-42-167D Cinch Lake MG-Calcite 11.9 -2.4 330 7.2 -4.9
C-42-191 Cinch Lake Calcite 14.4 -2.1 330 9.6 -4.6
C-42-191D Cinch Lake Calcite 14.5 -2.3 330 9.7 -4.7
M51-5996-MAT Cinch Lake Dolomite 22.2 -1.8 330 17.4 -4.2
M51-5996-MAT-D Cinch Lake Dolomite 22.1 -1.7 330 17.4 -4.2
VR Ace-Fay Calcite 12.9 -3.2 330 8.1 -5.6
VR_D Ace-Fay Calcite 12.9 -3.4 330 8.2 -5.8
VR-211 Ace-Fay Calcite 7.6 -4 330 2.8 -6.4
VR79 Ace-Fay Calcite 10.7 -5.8 330 5.9 -8.3
VR79D Ace-Fay Calcite 10.6 -5.8 330 5.9 -8.2
Volcanic-type U 5 mineralization
6122 Ace-Fay Dolomite 13.2 -1.1 320 8.1 -3.2
6122D Ace-Fay Dolomite 13.4 -1.1 320 8.2 -3.3
6139 Ace-Fay Dolomite 13.9 -1.2 320 8.7 -3.4
6139D Ace-Fay Dolomite 13.9 -1.2 320 8.7 -3.4
C-27-23 Cinch Lake Dolomite 20.8 -2.6 320 15.7 -4.7
C-27-262 Cinch Lake Calcite 9.8 -2.4 320 4.7 -4.6
C-27-319 Cinch Lake MG-Calcite 11.6 -2.7 320 6.4 -4.9
107

Sample ID Deposit Mineral
Mineral values Temperatures Fluid values
δ 18 O
V-SMOW
per mil
δ 13 C
V-PDB
per mil
o C
δ 18 O fluid
V-SMOW
per mil
δ 13 C fluid
V-PDB
per mil
C-27-319D Cinch Lake MG-Calcite 11.4 -2.6 320 6.3 -4.7
C-37-28 Cinch Lake Calcite 12.7 -1.7 320 7.5 -3.8
C-42-180 Cinch Lake Calcite 12.8 -2.1 320 7.6 -4.2
C-42-180D Cinch Lake Calcite 12.6 -1.9 320 7.5 -4.1
C-42-244-1 Cinch Lake Calcite 10.5 -1.9 320 5.4 -4.1
Athabasca-type U 6 mineralization
3705 Ace-Fay Dolomite 11.2 -1 235 3.3 -1.9
3705-D Ace-Fay Dolomite 11.2 -0.9 235 3.3 -1.9
Late calcite veins
C-09-181 Cinch Lake Calcite 14.6 -2.5 140 1.2 -0.5
C-16-220 Cinch Lake Calcite 12.8 -2.8 140 -0.6 -0.8
C-42-244 Cinch Lake Calcite 13.4 -6.4 140 0.02 -4.5
C-42-244D Cinch Lake Calcite 13.3 -6.5 140 -0.1 -4.6
Table 3.5. Measured δ 18 O and δ 13 C for calcite and calculated δ 18 O fluid and δ 13 C fluid values for
fluids in equilibrium with carbonate minerals for different generations of U mineralization in
the Beaverlodge area. Paragenesis of all phases analyzed is shown in Figures 3.3 and 3.4 and
data are plotted in Figure 3.8 (see the text for more details).
Syn-ore Cal 8 calcite in the major breccia-type U 4 yields a wide range of δ 18 O values
between 7.6 per mil and 22.2 per mil and δ 13 C values between -5.8 per mil and -1.6 per
mil (Table 3.5). These values are similar to O and C isotopic compositions of calcite
matrix from mineralized breccia reported by Tortosa (1983) at the Cenex deposit and to
values reported by Sassano (1972) for the type-C calcite in the Ace-Fay deposit that he
interpreted as syn-ore calcite-filling breccia. A formation temperature of 330°C was used
to calculate δ 18 O fluid and δ 13 C fluid values, which range from 2.8 per mil to 17.4 per mil and
-8.3 per mil to -4 per mil, respectively (Fig. 3.7; Table 3.5). The lowest δ 13 C fluid values
(Fig. 3.7) likely reflect the influence of a reduced C source probably originating from the
country rock with which the fluid has interacted (Fig. 3.7).
Syn-ore Cal 9 calcite sampled from the volcanic-type U 5 mineralization has δ 18 O
values ranging from 9.8 per mil to 20.8 per mil and δ 13 C values between -2.7 per mil and -
1.1 per mil (Table 3.5). Using a formation temperature of 320°C (Table 3.3), the
108

calculated δ 18 O fluid and δ 13 C fluid values of the fluid from which Cal 9 formed range from 4.7
per mil to 15.7 per mil and -4.9 per mil to -3.1 per mil, respectively (Fig. 3.7; Table 3.5),
with most of the δ 18 O fluid values between 5 per mil and 10 per mil. Syn-ore Cal 10 calcite
from the Athabasca-type U 6 mineralization yields δ 18 O values of 11.2 per mil and δ 13 C
values ranging from -1 per mil to -0.9 per mil (Table 3.5). Using a formation temperature
of ca. 235°C (Table 3.3), the calculated δ 18 O fluid and δ 13 C fluid values of the fluid are 3.3 per
mil and -1.9 per mil, respectively (Fig. 3.7; Table 3.5). Late Cal 11 calcite veins
crosscutting all rocks within the Beaverlodge area have δ 18 O values that range from 12.8
per mil to 14.7 per mil and δ 13 C values between -6.4 per mil and -2.5 per mil (Fig. 3.7;
Table 3.5). Using a formation temperature of 140°C, the calculated δ 18 O fluid and δ 13 C fluid
values are the lowest and give two components (Fig. 3.7). One has δ 18 O fluid and δ 13 C fluid
values ranging from -0.6 per mil to 1.2 per mil and -0.9 per mil to -0.5 per mil,
respectively, similar to isotopic compositions of seawater (Fig. 3.7). The second
component has much lower δ 13 C fluid and slightly higher δ 18 O fluid values, near -4.5 per mil
and 0 per mil, respectively.
3.4.3.2. Oxygen and hydrogen isotopic compositions of chlorite
Stable isotopic O and H compositions were determined for chlorite in textural
equilibrium with U for the granite-metasomatic, breccia, volcanic, and Athabasca-type U
mineralizations (Fig. 3.8; Table 3.6).
Syn-ore Chl 5 chlorite in the Gunnar deposit has δ 18 O values that range from 5.8 per
mil to 11.1 per mil and δ 2 H values between -75 per mil and -71 per mil (Fig. 3.8; Table
3.6). Assuming a formation temperature of 315°C (Table 3.3), Chl 5 chlorite formed in
109

equilibrium with a fluid having δ 18 O fluid values ranging from 6.1 per mil to 11.4 per mil
and δ 2 H fluid values from -48 per mil to -44 per mil (Fig. 3.8; Table 3.6).
Figure 3.8. Calculated δ 18 O and δ 2 H values of mineralizing fluids in equilibrium with chlorite
minerals. Samples of breccia and Gunnar-type have preferentially exchanged H-isotopes with
2 H-depleted, relatively modern meteoric water; their high δ 18 O values indicate alteration at
low fluid/rock ratios. The fields of various fluid reservoirs participating in hydrothermal ore
formation are also shown (e.g. Taylor, 1974; Faure, 1989; Cuney and Kyser, 2008).
Syn-ore Chl 7 chlorite in the breccia-type U 4 uraninite has a wide range of δ 18 O
values varying between 8.6 per mil and 17.1 per mil and δ 2 H values from -86 per mil to -
131 per mil (Table 3.6). The δ 18 O values are the highest compared to other types of
mineralization. Using a formation temperature of 330°C (Table 3.3), the calculated
δ 18 O fluid and δ 2 H fluid values for the fluid that formed Chl 7 chlorite range from 8.2 per mil to
110

16.6 per mil and -103 per mil to-59 per mil, respectively (Fig. 3.8; Table 3.6). The lowest
δ 2 H fluid values likely reflect the influence of modern meteoric water with which Chl 7
chlorite has reacted (Wilson and Kyser, 1987; Kyser and Kerrick, 1991).
Sample ID
Deposits
Metasomatic-type U3 mineralization
Mineral values Temperature Fluid values
δ 18 O
V-SMOW per
mil
δ 2 H
V-SMOW per
mil
o C
δ 18 O fluid
V-SMOW per
mil
δ 2 H fluid
V-SMOW per
mil
GN-06 Gunnar 9.2 -75 315 9.4 -48
GN-06B Gunnar 7.9 -71 315 8.1 -44
GN-36 Gunnar 5.8 -75 315 6.1 -48
GN-01 Gunnar 11.1 -71 315 11.4 -44
Breccia-type U4 mineralization
5810 Ace-Fay 8.6 -90 330 8.2 -63
5812 Ace-Fay 17.1 -104 330 16.6 -77
5812-Dup Ace-Fay 17.1 -104 330 16.6 -77
VR Ace-Fay 15 -108 330 14.6 -81
VR-2 Ace-Fay 14.2 -88 330 13.8 -61
CL47 Cinch Lake 15.4 -99 330 14.9 -72
6124 Cinch Lake 13.3 -130 330 12.8 -103
C-09-21 Cinch Lake 12.5 -86 330 12.1 -59
C-09-21S Cinch Lake 12.5 -99 330 12.1 -72
C-37-128 Cinch Lake 9.9 -109 330 9.5 -82
Volcanic-type U5 mineralization
CL Cinch Lake 10.4 -126 320 10.2 -99
CL-19 Cinch Lake 9.2 -101 320 9 -74
CL-19S Cinch Lake 9.2 -113 320 9 -86
CL-25 Cinch Lake 6.8 -104 320 6.6 -77
CL-25B Cinch Lake 8.9 -94 320 8.7 -67
CL-48 Cinch Lake 6.4 -71 320 6.2 -44
CL-48b Cinch Lake 7.3 -75 320 7.1 -48
CL-49 Cinch Lake 7.3 -99 320 7.1 -72
CL-55 Cinch Lake 7.3 -79 320 7.1 -52
CL-55S Cinch Lake 7.3 -93 320 7.1 -66
CL-64 Cinch Lake 6 -82 320 5.8 -55
Cl-64B Cinch Lake 10.4 -97 320 10.2 -70
F19-08 Ace-Fay 6.9 -100 320 7.1 -73
F230-30 Ace-Fay 8.3 -72 320 8.5 -45
F230-24 Ace-Fay 9.2 -79 320 9.4 -52
F19-09 Ace-Fay 9.3 -98 320 9.5 -71
Athabasca-type U6 mineralization
F230-14a Ace-Fay 3.5 -67 235 2.2 -40
F230-14b Ace-Fay 2.8 -65 235 1.5 -38
F230-14c Ace-Fay 5.2 -71 235 3.8 -44
F230-25 Ace-Fay 3.5 -63 235 2.2 -36
F230-25 Dup Ace-Fay 3.5 -68 235 2.2 -41
F230-46 Ace-Fay 7.7 -87 235 6.3 -60
F230-31 Ace-Fay 4.1 -68 235 2.8 -41
Table 3.6. Measured δ 18 O and δ 2 H for chlorite and calculated δ 18 O and δ 2 H values for fluids
in equilibrium with chlorite minerals from different generations of U mineralizing events in
the Beaverlodge area. Temperatures used to calculate the fluid values are derived from the
chlorite chemistry (see Table 3.3).
111

Syn-ore Chl 8
chlorite sampled from the volcanic-type U 6 mineralization has a
narrow range of δ 18 O values between 6 per mil and 10.4 per mil and a wide range of δ 2 H
values comprising between -126 per mil and -71 per mil (Table 3.6). Using a formation
temperature of 320°C (Table 3.3), δ 18 O fluid and δ 2 H fluid values for the equilibrium fluid
range from 5.8 per mil to 10.2 per mil and -99 per mil to -44 per mil, respectively (Fig.
3.8; Table 3.6). Chl 8 chlorite also records late alteration associated with the influence of
modern meteoric water (Fig. 3.8). In contrast, Syn-ore Chl 9 chlorite in Athabasca-type U 6
mineralization has the lowest δ 18 O values that range from 2.8 per mil to 7.7 per mil and
δ 2 H values comprising between -87 per mil and -63 per mil (Table 3.6). These values
indicate formation in equilibrium with brines having δ 18 O fluid values of 1.5 per mil to 6.3
per mil and δ 2 H fluid values of -60 per mil to -38 per mil based on a formation temperature
of 235°C (Fig. 3.8; Table 3.6). The calculated values of δ 18 O fluid and δ 2 H fluid are similar to
those from unconformity-type U mineralization in the proximal Athabasca Basin (Wilson
and Kyser, 1987; Kotzer and Kyser, 1995).
3.4.4. Rare earth elements (REE) geochemical characteristics of the U mineralization
REE contents of uraninite can constrain the origin and evolution of mineralizing
fluids (Alexander et al., 2010; Mercadier et al., 2011). Based on REE patterns, several
distinctions can be made between different types of U-mineralizing events. For example,
the REE contents in the granite-related metasomatic-type U 3 uraninite at Gunnar are high
(17834 ppm, Tables 3.7 and 3.8; Fig. 3.9B) and chondrite-normalized REE patterns
indicate a slight LREE enrichment (La/Yb) N =5.8, Figs. 3.9A and 3.10A) and pronounced
negative Eu and Ce anomalies (Eu/Eu*=0.1 and Ce/Ce*=0.1, Fig. 3.10A). In contrast, U 2
112

uraninite from the early tensional vein-type has LREE enrichment (La N /Yb N =14.4) but
low total REE contents (2386 ppm, Tables 3.7 and 3.8, Fig. 3.10B). The slope of the
chondrite-normalized pattern is steep (LREE/HREE=9.7), with slight negative Eu
(Eu/Eu*=0.6) and Ce (Ce/Ce*=0.7) anomalies (Fig. 3.10B). The total REE content in the
breccia-type U 4
uraninite, the most significant uranium mineralization, is the highest
(15848 ppm, Tables 3.7 and 3.8, Figs. 3.9B and 3.10C) with chondrite-normalized REE
patterns with a gentle slope (LREE/HREE=4.4), LREE fractionation (La/Yb) N =3.7; Figs.
3.10C and 3.10D), a negative Eu anomaly (Eu/Eu*=0.7), and a poorly defined Ce anomaly
(Ce/Ce*=0.9).
A
B
C
D
113

Figure 3.9. Binary diagrams showing chondrite normalized REE compositions of different
generation of uraninite A. Plot of (Yb) N vs (La/Yb) N , B. Plot of ΣREE vs LREE, C. Plot of
(La/Sm) N vs (La/Yb) N , D. Plot of ΣREE vs LREE/HREE.
The average total REE concentration in mafic dikes in the Martin Lake Basin is low
(ΣREE=378 ppm, Tables 3.7 and 3.8; Figs. 3.9B and 3.9D), with a pronounced LREE
enrichment (La N /Yb N =33.6) and slight negative Ce (Ce/Ce*=0.9) and Eu (Eu/Eu*=0.8)
anomalies (Fig. 3.10G). The U 5 uraninite from the volcanic-type has low REE contents
(ΣREE=4158 ppm) (Tables 3.7 and 3.8; Figs. 3.9B and 3.D) with pronounced LREE
enrichment (La N /Yb N =28.2) and negative Ce (Ce/Ce*=0.7) and Eu (Eu/Eu*=0.7)
anomalies (Table 3.7, Figs 10E and 10F). Chondrite-normalized REE patterns have a high
LREE/HREE ratio of 18, which is similar to patterns in mafic dikes (Fig. 3.10G).
Chondrite-normalized (La/Sm) N and (Tb/Yb) N and the ratio LREE/HREE are similar in
both mafic dikes and U 5 uraninite (Table 3.7), suggesting a genetic relationship.
Mineralisation Type n ΣREE ΣLREE ΣHREE LREE/HREE Eu/Eu* (La/Yb)N (La/Sm)N (Tb/Yb)N (Yb)N
Metasomatic 3 17834 2162 1653 7.2 0.1 19.5 5.0 1.6 192.2
Early Tensional vein 5 2386 2162 125 11.1 0.6 14.3 7.4 1.1 16.8
Breccia-type 12 15848 12021 2493 4.5 0.7 4.2 2.0 1.3 372.2
Volcanic-type 14 4158 3897 267 16.6 0.7 25.9 12.6 1.2 23.5
Mafic dyke 10 378 359 19 18.6 0.8 33.6 4.7 2.1 1.7
Athabasca-type 7 9497 8882 479 16.0 0.6 11.4 3.5 1.4 70.2
Table 3.7: Characteristic of REE compositions uraninite for different generations of U
mineralization in the Beaverlodge area. (LREE/HREE)=chondrite-normalized
(La+Ce+Nd)/(Dy+Er+Yb); Eu*=theoretical value for no chondrite-normalized anomaly. n=
number of analyses.
114

A
B
C
D
E
F
G
H
115

Figure 3.10. Chondrite-normalized REE patterns in uraninite from U deposits of the
Beaverlodge area. A: Metasomatic-type U 3 (Sample 6134, Gunnar Deposit), B: Early veintype
U 2 (Sample 6122, Ace Deposit), C: Breccia-type U 4 (Sample 5812, Ace-Fay deposit), D:
Breccia-type U 4 (Sample 90085, Ace-Fay deposit), E: Volcanic-type U 5 (Sample 6120, Ace Fay
deposit), F: Volcanic-type U 5 (Sample 6137, Gunnar deposit), G: Mafic dike, H: Athabascatype
U 6 (Sample 3705, Ace deposit).
The U 6 uraninite that has the same timing as the Athabasca-type mineralization is
LREE enriched (La N /Yb N =10.2) with a moderate total REE content (9497 ppm; Tables 3.7
and 3.8). Chondrite-normalized REE patterns have a negative Eu anomaly (Eu/Eu*=0.6)
and a positive Ce anomaly (Ce/Ce*=1.5) (Fig. 3.10H). This pattern differs from that of
uraninite from high-grade mineralization in the eastern Athabasca Basin (Mercadier et al.,
2011), indicating that fluids in the northern part of the basin had different REE
geochemistry.
Type Sample ID La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
Metasomatic 6134-12 3729.8 1650.0 1505.6 7426.5 1744.4 66.4 1281.9 156.4 875.6 162.7 408.2 57.3 374.7 42.9
Metasomatic 6134-10 3526.3 1739.6 1491.9 7088.4 1601.7 62.4 1204.1 150.2 867.6 158.7 406.4 57.5 383.7 47.0
Metasomatic 6134-9 3031.1 1371.2 1162.3 5581.2 1342.3 52.1 973.2 123.3 728.4 131.3 339.9 48.7 312.2 37.6
Early vein 6122-18 640.2 736.2 87.0 342.2 66.9 11.5 64.0 8.9 60.4 12.8 36.9 5.0 30.7 4.5
Early vein 6122-17 630.9 835.5 92.8 382.0 64.0 13.3 64.0 8.7 58.9 11.8 32.8 4.3 27.5 3.6
Early vein 6122-19 675.6 863.8 95.6 408.3 65.3 11.9 57.4 7.9 52.1 12.7 34.8 5.4 31.9 4.1
Early vein 6122-21 680.9 867.5 95.9 391.4 66.9 13.6 67.4 7.7 59.9 10.5 32.3 3.8 27.8 3.7
Early vein 6122-22 822.9 1028.4 119.2 605.6 77.9 15.6 87.3 11.0 73.1 14.7 40.1 5.3 28.3 5.4
Breccia 5812_9 3508.8 8452.6 1036.5 4487.9 1258.8 192.6 1199.0 263.1 2017.8 401.3 1249.2 246.5 1867.3 221.7
Breccia 5812_3 4789.0 7968.2 903.1 3369.1 866.5 174.9 732.5 138.8 972.8 187.4 540.7 72.6 419.7 49.9
Breccia 5812_8 3536.8 7751.8 886.5 3322.5 683.1 160.7 566.2 104.4 714.0 129.0 368.3 56.0 370.9 43.5
Breccia 90085-5 2220.0 4653.4 599.9 2661.6 720.6 166.4 702.8 119.5 793.6 148.0 386.3 53.4 344.4 38.5
Breccia 5812_5 1769.4 6915.6 919.6 3302.0 614.1 121.5 394.1 79.4 559.1 103.9 302.8 48.7 339.1 39.2
Breccia 90085-10 1731.2 3981.7 514.2 2460.9 649.1 176.7 734.0 120.1 817.5 155.1 420.8 55.4 339.7 42.1
Breccia 90085-11 2310.0 4095.9 550.8 2804.5 831.6 196.1 948.6 180.0 1319.4 257.1 726.6 104.3 669.1 81.6
Breccia 90085-2 2015.6 3993.8 542.6 2464.9 673.4 168.2 676.0 116.1 800.5 145.7 383.5 54.1 337.1 38.6
Breccia 5812_2 2010.3 4375.0 616.7 2937.2 790.8 173.4 778.6 141.6 943.7 187.5 527.6 68.6 426.6 52.6
Breccia 90085-7 1888.5 3574.8 458.6 2139.1 593.9 158.7 691.8 115.8 791.9 157.3 420.7 56.1 358.1 41.2
Breccia 90085-1 1676.0 3607.3 476.3 2106.9 532.0 128.2 522.9 85.5 571.7 108.0 293.9 38.6 234.6 28.3
Breccia 90085-4 1678.9 3252.0 426.7 1843.8 506.2 120.4 501.3 79.0 508.7 100.7 256.3 34.4 213.3 24.3
Volcanic 6120-11 1833.3 2728.2 230.0 632.1 57.7 14.0 54.5 7.0 46.4 9.9 27.5 3.8 24.6 3.4
Volcanic 6120-8 1713.6 2312.2 188.7 550.8 62.5 14.6 69.8 9.9 65.0 13.6 39.2 5.0 29.8 4.4
Volcanic 6139-6 1571.9 1978.3 172.3 586.1 99.7 24.3 106.2 17.7 129.8 25.9 69.5 9.9 61.0 8.1
116

Volcanic 6120-5 1553.0 2260.4 186.0 519.3 51.4 11.9 52.9 7.5 50.2 10.5 29.2 3.9 24.5 3.4
Volcanic 6120-1 1502.3 2267.9 181.4 471.9 42.4 10.5 44.8 5.8 39.3 8.4 25.0 3.4 22.2 3.1
Volcanic 6139-4 1796.1 1485.6 129.3 469.2 72.8 16.6 78.9 12.0 84.2 17.3 46.2 6.5 43.9 4.8
Volcanic 6120-4 1414.3 2016.8 154.9 391.0 33.9 7.9 35.9 4.8 33.3 7.1 20.7 2.8 18.6 2.8
Volcanic 6120-10 1287.5 1866.2 151.3 393.7 37.6 9.5 41.6 5.6 38.8 8.1 23.2 3.1 20.6 3.0
Volcanic 6139-3 1533.8 1271.3 122.0 460.2 82.7 18.3 94.7 14.4 101.7 20.7 55.4 7.9 49.4 6.0
Volcanic 6139-2 1384.1 1280.7 126.5 498.2 89.2 19.4 97.0 14.3 99.2 19.9 53.5 7.2 44.6 5.7
Volcanic 6139-9 1197.1 1228.3 127.1 521.8 100.5 22.7 118.0 16.6 113.1 22.4 59.4 7.7 49.8 6.3
Volcanic 6139-7 1100.9 1179.8 112.0 472.2 88.7 20.6 104.2 14.4 96.6 19.3 49.9 6.4 39.8 5.2
Volcanic 6120-3 1127.4 1478.6 112.0 310.7 34.2 8.6 46.6 6.2 43.0 9.7 27.9 3.7 24.3 3.7
Volcanic 6139-5 1032.3 1127.3 115.5 480.0 89.9 19.1 91.8 13.9 92.5 19.5 49.8 6.9 43.4 5.3
Athabasca 3705-4 1948.2 6666.6 601.0 2047.4 347.8 58.3 220.0 38.2 244.7 43.8 125.7 18.4 117.8 14.4
Athabasca 3705-3 1775.0 6435.4 573.9 1869.6 312.8 53.4 214.5 36.0 233.2 41.4 121.2 16.3 110.0 14.4
Athabasca 3705-12 1571.3 5964.9 511.0 1625.1 258.8 41.3 145.7 26.8 178.6 29.6 80.7 12.6 86.7 9.8
Athabasca 3705-2 1175.1 4674.0 468.8 1617.6 288.7 49.1 172.4 31.2 197.3 35.5 100.5 14.9 91.1 10.9
Athabasca 3705-6 1157.4 4863.5 442.2 1411.6 215.9 38.3 140.8 26.9 182.0 30.1 93.9 14.2 101.3 11.6
Athabasca 3705-1 1459.7 4766.3 390.1 1181.7 248.0 41.6 152.1 29.1 198.6 35.6 92.2 15.3 87.6 10.9
Athabasca 3705-5 893.9 2913.2 237.8 844.7 115.8 20.4 69.4 12.3 74.0 13.7 35.1 5.1 34.0 3.8
Mafic dike RM-18 197.55 381.58 41.57 148.96 20.63 4.57 12.12 1.07 5.05 0.8 1.99 0.25 1.48 0.28
Mafic dike RM-17 108.28 219.98 24.84 90.07 14.25 3.37 9.64 1.03 5.33 0.9 2.32 0.3 1.87 0.37
Mafic dike RM-21 93.24 194.96 22.8 86.25 13.31 3.08 8.87 0.92 4.75 0.83 2.09 0.29 1.65 0.3
Mafic dike RM-32 93.16 186.32 21.36 79.32 12.77 2.93 9.15 1 5.38 0.94 2.4 0.32 1.98 0.39
Mafic dike RM-35 71.47 150.81 17.32 65.26 11.27 2.27 8.46 1.03 5.75 1.09 2.97 0.43 2.67 0.52
Mafic dike RM-23 70.17 136.46 15.08 56.4 8.79 2.14 6.32 0.71 4.01 0.72 1.97 0.27 1.59 0.32
Mafic dike RM-34 56.31 110.7 12.49 46.47 7.7 1.97 6.12 0.72 4.16 0.74 2.06 0.27 1.68 0.33
Mafic dike RM-36 55.95 109.47 12.28 45.24 7.71 1.96 5.98 0.73 4.14 0.76 2.06 0.29 1.72 0.34
Mafic dike RM-26 54.5 105.53 11.89 43.91 7.33 1.79 5.79 0.69 3.95 0.7 1.89 0.26 1.6 0.31
Mafic dike RM-33 53.57 105.07 11.87 44.59 7.25 1.91 5.79 0.7 4.01 0.75 1.99 0.28 1.67 0.34
Table 3.8. REE contents of uraninite from different generations of U deposits in the
Beaverlodge area. Values for the mafic dike are from Moreilli et al. (2009). Data are plotted
in Figure 3.10.
3.5. Discussion
Synthesis of the petrographic, structural, geochronologic, and geochemical data
reveals the nature and sequence of alteration and mineralization leading to the formation
of U deposits in the Beaverlodge area (Table 3.9). This sequence is geochemically and
structurally complex, involving multiple overprinting events of deformation, hydrothermal
alteration, and U mineralization occupying structurally disturbed zones created by ductilebrittle
and brittle deformation that reactivated early ductile shear zones (Fig. 3.11).
117

Retrograde
metamorphism
Early vein
-type
Metasomatic
-type
Breccia-type
Volcanic
-type
Athabasca
-type
Deposits All deposits Ace-Fay Gunnar All deposits
Ace-Fay-Cinch
Lake-Gunnar
Ace Fay,
Martin Lake
Mineral and ore
assemblage
Chl 1 -Hem 1 -Src 1 U2 -Chl 4 -Cal 4 - U 3 -Chl 5 -Cal 5 -Ttn 2
U 5 -Chl 8 -Cal 9 -
U 4 -Br 1 -Chl 7 -Cal 8 - Hem 7 -Ap 1 -Ttn 3 - U 6 -Chl 9 -Cal 10 -
Hem 4 -Mnz 1 -Hem 5 Hem 6 Hem 8
Mnz 2
Age of formation

of the Arrowsmith Orogen at ca. 2.35 Ga (Berman et al., 2005, Dieng et al., 2011).
Metamorphic retrogression continued during exhumation to shallower crustal depths
resulting in greenschist facies conditions wherein retrograde Chl 1
chlorite replaced
regional metamorphic Bt 1 biotite down to ca. 200°C. Chl 1 chlorite reflects exhumation and
retrograde metamorphism to lower greenschist facies in the basement rocks during the late
stages of the Arrowsmith Orogen (Hartlaub et al., 2007; Berman et al., 2010).
Metamorphic-hydrothermal fluids associated with Chl 1
chlorite are relatively Ca-rich,
have high F and Mg contents and likely result from interaction with, or metamorphic
hydration of, Ca-Mg-F-rich rocks of the basement rocks.
Shear zones were reactivated at shallower levels resulting in overprinting of
mylonite by cataclasite and early tensional veins at ca. 2.29 Ga (Dieng et al., 2011).
Petrographic observations indicate that U 1
uranium mineralization occurs as fine
disseminations in the cataclasite matrix and is cut by early tensional Qtz 3 +Cal 3 -±U 2 veins
(Fig. 3.11B). Syn-ore Cal 4 calcite associated with U 2 uraninite at the Ace deposit has δ 13 C
and δ 18 O values that are consistent with fluids derived from retrograde metamorphic
processes. Syn-ore Chl 4 chlorite chemistry indicates that fluids associated with U 2
mineralization formed at ca. 310 o C and were Ca-F-Mg-rich. The compositional similarity
between syn-ore Chl 4 chlorite and retrograde Chl 1 chlorite indicates that U-bearing fluids
derived from retrograde metamorphic processes during exhumation and erosion during the
post-Arrowsmith Orogen may have been involved in the formation of U 2 mineralization.
Hydraulic fracturing in response to fluid generation via decompression and hydration was
probably the main mechanism of the early tensional vein formation. The high F and Ca
119

contents in syn-ore Chl 4 chlorite indicate that uranyl-carbonate-fluoride complexes were
the most likely form of U 2 complexes into solutions. The vein-forming fluid may have
been driven into these fractures by suction pump processes (Sibson, 1987). The associated
pressure decrease and fluid decompression during fracturing were sufficient to change the
stability of the carbonate complexes, decrease the temperature of the fluids and likely
promoted U 2 uraninite precipitation into the fracture systems (Fig. 3.11B).
120

Figure 3.11. Conceptual genetic model for U mineralization in the Beaverlodge area. A:
Deposition of the Murmac Bay Group sediments in a tectonically active fault-bounded basin is
followed by mylonitization during the Arrowsmith Orogen. B: Mylonites reactivated during
late stages of the Arrowsmith Orogen resulting in formation of cataclasite and early tensional
vein-type U 2 mineralization. Hydraulic fracturing in response to fluid generation via
121

decompression and hydration reactions was the mechanism of veins formation. U was
transported as uranyl-carbonate-fluoride complexes. C: At Gunnar, U 3 was derived from
magmatic fluids from the Gunnar granite. PO -3 4 and F - were important ore transporting
complexes. D: Reactivation of fault zones during early regional metamorphism of the Trans-
Hudson or post-peak Thelon-Taltson Orogen resulted in massive brecciation at shallow
structural levels. Metamorphic-hydrothermal U-mineralizing fluids derived from dehydration
of hydrous minerals during metamorphism ascended upward along deep fractures and
decompression caused decrease in the solubility of the carbonate complexes promoting U
deposition. E: During the Paleoproterozoic, the Martin Lake Basin and associated alkaline
mafic dikes formed and hydrothermal U 5 -mineralizing solutions resulted in magmatichydrothermal
degassing along pre-existing fractures. F: Ore-forming brines from the
Athabasca Basin descended along fractures in the basement rocks and U 6 deposition was via
reduction through interaction between oxidizing basinal brines and reduced metamorphic
basement lithologies. G: Post-ore incursion and circulation of meteoric water through
structurally reactivated fault zones that remain a zone of preferential fluid circulation. H:
Erosion of the Athabasca and part of Martin Lake basin rocks and weathering of the deposit
resulted in the recent formation of secondary uranium minerals and late alteration veins.
Deposition of the 2.33 Ga Murmac Bay Group sediments (Hartlaub and Ashton,
1998) was followed by intrusion of the ca. 2321±3 Ma Gunnar granite (Evoy, 1969;
Hartlaub et al., 2004a), which hosts the granite-related metasomatic-type U 3 uranium
mineralization (Fig. 3.11C). The timing of this mineralization is constrained between the
age of the granite (ca. 2321±3 Ma) and the brecciation event (1850 Ma; Dieng et al., 2011)
that overprinted the granite-related U-mineralization at Gunnar. δ 18 O, δ 13 C and δ 2 H
isotopic compositions of syn-ore Cal 5 calcite and Chl 5 chlorite (Figs. 3.7 and 3.8) indicate
that U 3 mineralization has ore-forming components consistent with derivation from
magmatic fluids (Fig. 3.11C). The strong negative Eu anomaly in U 3 uraninite indicates
retention of plagioclase during albitization of the granite. Collectively, these results
demonstrate that fluids involved in the metasomatic alteration of the Gunnar granite could
122

e the same as the U 3 -mineralizing fluid. Therefore, the source of U 3 uraninite in the
granite-related mineralization was likely the Gunnar granitic rock itself. U 3 uraninite could
have been transported by cooling exsolved residual magmatic hydrothermal fluid at ca.
315 o C during magmatic-hydrothermal degassing and deposited in voids left after Qtz 1
quartz and Cal 5 calcite dissolution. The negative chondrite normalized Ce anomaly could
be related to Ce-absorption in Mnz 1 monazite during U 3 uranium precipitation. The high
REE content in the metasomatizing brine is likely related to trace element fractionation
into the fluid during its separation from the granitic melt (e.g. Giere, 1986). Abundant F
within the syn-ore minerals and the presence of Mnz 1 monazite intergrown with U 3
uraninite, suggest that P and F were important ore transporting complexes and that U 3
uranium transfer into the exsolved magmatic-hydrothermal solutions was as uranylfluorine-phosphate
complexes (e.g. U(HPO 4 ) 2 and UF 4 ). The negative chondrite
normalized Eu anomaly (Fig. 3.10A) indicates that the hydrothermal mineralizing fluid
was reduced and that magmatic-fluid degassing processes may have caused the loss of a
large volume of CO 2 that destabilized U and REE complexes, thereby promoting the
deposition of U 3 mineralization.
The style of the granite autometasomatism and the mechanism of ore-forming
processes are similar to deposits in the Xiazhuang district (e.g. Zhushanxia, and Xiwang
deposits), southern China (Du Letian, 1986), the albitized granite-hosted U mineralization
in Brazil (Porto da Silveira et al., 1991) and France (Leroy, 1978). At the Gunnar deposit,
U 3 mineralization is later overprinted by the breccia- (U 4 ) and volcanic-type (U 5 )
123

mineralizations, which upgraded the deposit significantly. The breccia-type U 4
mineralization accounts for the majority of the U in the Gunnar deposit.
3.5.2. Formation of breccia-type U deposits, the major U mineralization
Massive brecciation and formation of the breccia-type main U 4 -mineralizing event at
1850 Ma is linked to reactivation of the fault zones during the post-peak Thelon-Taltson
Orogen or, more likely, early stages of the Trans-Hudson Orogen (Dieng et al., 2011)
(Fig. 3.11D). δ 18 O, δ 13 C and δ 2 H values of syn-ore Chl 7 chlorite and Cal 8 calcite are
consistent with the ore-forming fluid as predominantly metamorphic in origin (Figs. 7 and
8). Syn-ore Chl 7 Chlorite crystal chemistry indicates that the fluid formed from Ca-Na-Fcontaining
metamorphic brine at ca. 330 o C also had relatively high Fe contents. These
fluids were likely derived from dehydration of hydrous minerals and ascended upward
along deep and large fracture systems and dilatant jogs that resulted from brittle
reactivation of early ductile shear zones, thus providing pathways for metamorphichydrothermal
mineralizing solutions (Fig. 3.11D). REE enrichment in U 4 uraninite,
abundant Cal 8 calcite in textural equilibrium with U 4 uraninite, and F in Chl 7 chlorite
indicate that U 4
uraninite transfer into the metasomatizing solutions was possibly as
uranyl-carbonate-fluoride complexes. Experimental results of Bilal and Koss (1980a)
demonstrate that both F - and CO 2- 3 can be effective ligands for complexing REE and U in
metasomatic fluids. The association of U 4 uraninite and Cal 8 calcite in the ore assemblage
(Fig. 3.4G) suggests that the fluids were likely alkaline (Cuney and Kyser, 2008). The
occurrence of both Br 1 brannerite and U 4 uraninite in the ore assemblage is similar to
others metamorphic-related U systems such as Valhalla (Polito et al., 2007) and the
124

Ukraine (Cuney and Kyser, 2008) wherein both U and Ti are mobilized in F-rich and CO 2 -
rich fluids (Hynes, 1980; Gieré, 1990). U 4 uranium precipitation in the breccia system is
likely caused by a decrease in the solubility of the carbonate complexes resulting from a
loss of CO 2 and a decrease in temperature caused by fluid decompression during
brecciation so that pressure and temperature conditions may have been the most dominant
factors controlling U 4 uranium mineralization. However, U transported by F-rich oxidized
fluids in metamorphic-related U-systems may be deposited via reduction reactions
(Skirrow et al., 2009) as the U 4 -mineralizing fluid reacted with reducing Ca-Fe-rich
metamorphic host rocks, resulting in the following reaction (Langmuir, 1978):
2Ca 2+ + UO 2 (CO 3 ) 3
4-
+ 2Fe 2+ +4HCO 3
-
= UO 2+ ↓ + Fe 2 O 3 ↓ + 2CaCO 3 ↓ + 2H 2 O + 5CO 2 ↑.
This process may explain the abundance of Hem 6 hematite associated with U 4 uraninite,
the Cal 8 calcite alteration in the breccia matrix, and the Fe-rich Chl 7 chlorite. In hightemperature,
reduced F-rich metamorphic-related U-systems, the activity of calcium and
pH may be more important than redox in controlling U deposition due to the low
solubility of fluorite (Skirrow et al., 2009).
These results corroborate the findings of Hoeve (1982) who proposed that the
Beaverlodge U deposits may represent a Na-Ti-U style mineralization related to Nametasomatism
during regional metamorphism by the Trans-Hudson Orogen. He suggested
that the resulting Na-alteration involving addition of Na and Ca and loss of K, Mg, Fe, Ti,
and U from the rocks are related to interaction between metamorphic-related hydrothermal
fluids and country rocks. The mineralizing brine deposited the U mineralization in fracture
and breccia systems at structurally shallow levels. Others have also proposed a
125

metamorphic origin of the main U 4 mineralizing event. Tremblay et al. (1972) suggested
that rocks of the Beaverlodge area may represent previously U-rich regions that were
leached during metamorphic-hydrothermal alteration during late Trans-Hudson
granitization processes and that the U mineralization was deposited along major fault
zones. Rees (1992) proposed a metamorphic origin for fluids associated with the lode-gold
quartz vein mineralization at the Nicholson deposit, which formed at ca. 1.85-1.84 Ga at
temperatures of ca. 300-400 o C. His results demonstrate that Au gold and U mineralization
likely formed from the same mineralizing event.
A strong structural control is reported in most metamorphic-related U systems, with
U commonly hosted by reactivated ductile to brittle-ductile fault zones (Cuney and Kyser,
2008). Skirrow et al. (2009) suggest that fluids in these systems are saline Na-Ca brines
that were F-rich and CO 2 -bearing. Such U deposits formed from fluids of metamorphicdehydration
origin and appear to be rare and of low grade and tonnage (Plant et al., 1999).
The relatively low oxidation state of such fluids may explain why these systems are not
associated with significant U mineralization. The Beaverlodge U deposits are therefore,
similar to these metamorphic-related U mineralization systems associated with Nametasomatism
(Cuney and Kyser, 2008). Examples include the Krivoy-Rog district in
Ukraine (Belevtsev and Koval, 1968), the Kurupung district in Guyana (Cinelu and
Cuney, 2007) and Skuppesavon in Sweden (Smellie and Laurikko, 1984). Therefore, these
deposits could be related to the global 1.9-1.75 Ga alkali-metasomatism associated with
the plate tectonic-scale collisional orogenesis culminating with the Nuna supercontinent
assembly (Cuney, 2010; Evans et al., 2010).
126

3.5.3. Later basin-related U mineralization
Formation of the Martin Lake Basin (Langford, 1981; Mazimhaka and Hendry,
1984) and associated 1818±4 Ma alkaline mafic dikes (Morelli et al., 2009) is coincident
with periods of active tectonism related to back-arc extension following peak Trans-
Hudson Orogen (Hoffman, 1989; Corrigan, 2009). Extrusion of mafic dikes is associated
with the ca. 1820 Ma volcanic-type U 5 -mineralization (Dieng et al., 2011) identified at the
Cinch Lake, Ace-Fay, and Gunnar deposits (Fig. 3.11E). Syn-ore Chl 8 chlorite and Cal 9
calcite have δ 18 O, δ 13 C and δ 2 H values typical of magmatic fluids (Fig. 3.8) that are likely
exsolved from mafic dikes during their emplacement. Chl 8
chlorite crystal chemistry
indicates that the U 5 -bearing hydrothermal fluid formed at ca. 320°C from an Mg- and Ferich
fluid. REE patterns of U 5 uraninite are similar to those in the mafic dikes and there is
a close spatial field relationship between mafic dikes and fractures hosting U 5 uraninite.
Therefore, during the mafic dikes intrusion and subsequent magmatic-hydrothermal
degassing, pre-existing fractures would have provided pathways for U 5
uranium
mineralizing solutions. Chondrite normalized REE patterns of U 5 uraninite indicate that
Eu is relatively more depleted in U 5 uraninite than in mafic dikes, suggesting that the
exsolved fluid changed from oxidized to less so during U 5 uranium deposition. The
shallow structural levels of emplacement and the presence of Mn-oxides and Hem 7
hematite alteration associated with U 5
uraninite indicate that during early stages, the
hydrothermal fluids were oxidized and capable of transporting U. In such an oxidizing
environment with intermediate pH conditions (4-8) and temperatures near 320°C, uranylphosphate
complexes were likely the most stable (Langmuir, 1978). This is corroborated
127

y the abundance of Ap 1 apatite and Mnz 2 monazite intergrown with U 5 uraninite in the
ore assemblage, suggesting that U 5 uraninite was probably transported in its oxidized state
as U 6+ primarily as uranyl-phosphate complexes (e.g. UO 2 (HPO 4 ) -2 2 ). Therefore, changes
in the pH or Eh state of the mineralizing solution through interaction between the
oxidizing hydrothermal brine and the reduced metamorphic host rocks was likely the key
process leading to U 5 uranium deposition. Destabilization of the aqueous uranyl-phosphate
complexes have resulted in the phosphate-bearing minerals intergrown with U 5 uraninite.
During the late Paleoproterozoic, the Athabasca Basin formed at ca. 1750 Ma
(Kyser et al., 2000) following exhumation of the Martin Lake Basin rocks. Tectonic
reactivation along fault zones during the Mesoproterozoic Mazatzal Orogen (Labrenze and
Karlstrom, 1991; Eisele and Isachsen, 2001) caused minor fracturing, deformation of the
basin and deposition of the 1620 Ma Athabasca-type U 6 mineralization observed in the
Ace-Fay and Martin Lake deposits (Dieng et al., 2011). Syn-ore Chl 9 chlorites formed
from fluids with δ 18 O and δ 2 H values (Fig. 3.8) identical to those of the unconformityrelated
U-deposits in the Athabasca Basin (e.g. Fayek and Kyser, 1997; Cuney and Kyser,
2008). The crystal chemistry of syn-ore Chl 9 chlorite indicates that fluids related to U 6
uraninite formed at ca. 235°C also identical to those of the Athabasca brines. U 6 uraninites
have total REE contents intermediate to those of U 4 and U 5 uraninites and are LREE
enriched, suggesting that these uraninites may have originated from an environment where
both U 4 and U 5 uraninites were remobilized. These observations suggest that this event
may be related in part to remobilization of pre-existing U mineralization into late fractures
from fluids that formed the unconformity-type U-mineralization in the Athabasca Basin
128

(Alexandre et al., 2009). Positive chondrite normalized Ce anomaly in U 6 uraninite may
indicate destruction of monazite and incorporation of Ce into the mineralizing brine
(Kyser et al., 2003), but the similarity of the isotopic composition, temperature and timing
of fluid events, all suggest that U 6 mineralizing brines originated in the Athabasca Basin
and descended downward along fracture systems into the basement rocks (Fig. 3.11F).
Syn-ore Chl 9 chlorite and U 6 uraninite crystal chemistry indicate that F - , Chl - , CO 2- 3 , and
PO 4
3-
were likely present in the ore assemblage and could be effective ligands for
complexing U 6 (e.g. UO 2 F 2 , UO 2 Cl 2 , UO 2 (CO 3 ) 2- , and UO 2 (H 2 PO 4 ) 2 ). In oxidized aqueous
basinal brines with pH between 4 and 7.5, uranyl-phosphate complexes are the important
species (Cuney and Kyser, 2008), uranyl-carbonate complexes are dominant under
relatively oxidizing and near-neutral pH conditions and the chlorine- and fluorinecomplexes
are dominant in fluids under acidic conditions at temperatures up to 200°C
(Romberger, 1984; Kojima et al., 1994). Therefore, the key process controlling U 6
uranium deposition was likely reduction of the mineralizing solution through interaction
between the oxidizing basinal brines and the reducing metamorphic basement lithologies
(Hoeve and Quirt, 1984; Polito et al., 2005, 2006; Cuney and Kyser, 2008).
Destabilization of the aqueous uranyl complexes is indicated by syn-ore Cal 10 carbonate
alteration, high phosphate contents in U 6 uraninite and elevated values of fluorine and
chlorine in Chl 9 chlorite.
3.5.4. Late alteration events
Electron microprobe analyses indicate that Chl 5 , Chl 7 , and Chl 8
chlorites were
subsequently altered to low-temperature Mg-rich chlorite (Table 3.4) recording the effect
129

of late fluid events that have affected the deposits subsequent to their formation (Figs.
3.11F and 3.11E). These late events may represent incursion and circulation of meteoric
water through structurally reactivated fault zones (Kotzer and Kyser, 1995). This is
reflected in the hydrogen isotopic composition of Chl 7 and Chl 8 chlorites, which record
retrograde exchange of H-isotopes with relatively recent meteoric water having low δ 2 H
values (Fig. 3.8) (Kyser and Kerrich, 1991; Kotzer and Kyser, 1995). The preferential
exchange of hydrogen isotopes in Chl 7 and Chl 8 chlorites suggests that the fault zones
were active after U-mineralization and remain a zone of preferential fluid circulation (e.g.
Fayek and Kyser, 1997; Beyer et al., 2011).
3.6. Conclusions
This study demonstrates that the Beaverlodge area records ore-forming systems that
resulted from multistage deformation, hydrothermal alteration and U mineralization, and
modern meteoric fluid processes during protracted tectonic evolution. The main brecciatype
U 4 mineralizing event that affected all deposits in the Beaverlodge area formed from
Ca-Na-dominated metamorphic fluids at ca. 330 o C associated with metasomatism
accompanying the regional metamorphism of the Trans-Hudson Orogen or post-peak
Thelon-Taltson Orogen. The ore-forming fluids were likely derived from dehydration of
hydrous minerals and ascended upward along deep fracture systems that resulted from
brittle reactivation of early ductile shear zones. U 4
transfer into the metasomatizing
solutions was as uranyl-carbonate-fluoride complexes and precipitation in the breccia
systems by a decrease in the solubility of the carbonate complexes and temperature caused
by fluid decompression during brecciation. Pressure and temperature conditions were the
130

most dominant factors controlling U 4 uranium deposition. The style of the mineralization
process is similar to U deposits in northern Sweden, Ukraine, Brazil and Guyana, all of
which contain high grade U mineralization in zones of brecciation related to the global
1.9-1.75 Ga alkali-metasomatism during plate tectonic-scale collisional orogenesis
culminating with the Nuna supercontinent assembly. In the Beaverlodge area, brittle
reactivated ductile shear zones represent an exploration target for U mineralization.
However, the metamorphic origin of the main U mineralization with fluids incapable of
transporting significant amounts of U may indicate that these deposits have only marginal
potential to host economic U mineralization, and certainly they would be relatively lowgrade.
These U mineralization events are older than the unconformity-related U
mineralization in the overlying Athabasca Basin. Therefore, U mineralization in this older
successor basin would have been one potential source of U for the Athabasca Basin.
131

CHAPTER 4
FLUID EVOLUTION AND GENESIS OF URANIUM
MINERALIZATION IN THE SOUTH ALLIGATOR VALLEY AREA,
NORTHERN TERRITORIES, AUSTRALIA
Abstract
Uranium deposits in the South Alligator Valley Mineral Field, Northern Territories,
Australia, are hosted in deformed and metamorphosed volcanoclastic rocks and calcareous
and carbonaceous sedimentary units of the Koolpin Formation, at the unconformity with
overlying El Sherana Basin sandstones. The ore is confined to greenschist facies host rocks
that are cut by the El Sherana-Palette fault, a northwest-striking, southwest dipping and
dextral strike-slip fault system. Petrographic studies on polished thin sections combined
with electron microprobe analysis, stable isotope geochemistry, and geochronology of
uranium-bearing minerals at the El Sherana and Coronation Hill deposits have identified a
multistage fluid history, involving hydrothermal alteration and uranium mineralization.
The pre-ore stage mineralogy consists of sericite, quartz, chlorite, and calcite
alteration at temperatures at ca. 300°C, interpreted to result from regional greenschist
metamorphism of the basement rocks during the ca. 1860-1840 Ma Nimbuwah event and
prior to deposition of the ca. 1840-1830 Ma El Sherana Basin. The basement pre-ore
alteration is followed by diagenesis of the El Sherana Basin sediments by oxidizing low
latitude basinal brines that produced a kaolinite+quartz+hematite assemblage. The ore stage
of uranium, gold, and galena formed at ca. 1820 Ma from evolved basinal brines that
originated from the El Sherana Basin and descended downward into basement rocks along
132

fracture systems created by brittle reactivation of the El Sherana-Palette fault at
temperatures near 250°C. Syn-ore mineral crystal chemistry suggests that uranyl-fluoridechloride
and -phosphate were dominant ore transporting complexes. Interaction of
oxidizing basinal brines with reducing Koolpin Formation sediments led to deposition of
the ore metals. Uranium deposits of the South Alligator Valley Mineral Field can therefore,
be classified as unconformity-related uranium mineralization associated with the El
Sherana successor basin. Post-ore alteration is dominated by secondary uraninite along late
fractures, kaolinite and hematite alteration, and chlorite and calcite veins, which formed at
temperatures near ca. 100°C. Post-ore alteration occurred during major tectonic events
based on U-Pb and Pb-Pb dating of uraninite and was coincident with fluid flow induced by
both near and far-field tectonic events that altered much of the primary uraninite into
secondary uranium minerals.
Our results show that the age of the uranium deposits are older than previously
proposed and are also older than the unconformity-related uranium mineralization in the
Kombolgie Basin. Unconformity-related uranium mineralization is associated with basinal
brines from the Paleoproterozoic successor basin, thereby enhancing the uranium
prospectivity of the area.
4.1. Introduction
The South Alligator Valley Mineral Field (SAVMF), Northern Territories, Australia,
lies within a north-west-trending zone of folded and faulted Paleoproterozoic
metasediments (Fig. 4.1) exposed within the South Alligator Valley in the Pine Creek
Orogen (Needham et al., 1980, 1987, 1988; Needham and Stuart-Smith, 1985, Valenta,
133

1990, 1991; Wyborn et al., 1990). Historic exploration within the SAVMF resulted in the
discovery of several uranium deposits and occurrences. Nevertheless, the SAVMF is the
smallest uranium field in the Pine Creek uranium province (Fig. 4.1). Between 1956 and
1964 only 874 t of U 3 O 8 was mined from 14 deposits (Foy, 1975). Since the discovery of
unconformity-type uranium deposits in the Kombolgie Basin, research in the Pine Creek
Orogen has been focused on the large and higher grade deposits within the Kombolgie
Basin, which uncomformably overlies the successor El Sherana Basin (Friedmann and
Grotzinger, 1994). The character and formation of unconformity-related uranium deposits
associated with the younger Kombolgie Basin (Sweet et al., 1999) have been well
documented and a general genetic model proposed (e.g. Gustafson and Curtis, 1983; Polito
et al., 2004; 2005; Cuney, 2005). In contrast, uranium mineralization in the successor El
Sherana Basin has been less studied, despite several decades of intense exploration and
mining activities and the discovery of several uranium and precious metal deposits (e.g.
Needham and Stuart-Smith, 1987; Mernagh et al., 1994). Moreover, there is limited
information on the role of the successor basin and the key processes by which these
deposits formed. The U mineralization occurs in basement rocks beneath, and within, the
successor El Sherana Basin (e.g. Ayres et al., 1975; Mernagh et al., 1994) that is
stratigraphically older than, but spatially related to, the younger U-rich Kombolgie Basin
(e.g. Wilde, 1992; Polito et al., 2005). Whether these deposits are unconformity-related
associated with the successor basin or similar to those in the younger Kombolgie Basin is
inconclusive.
134

Figure 4.1. a) Geological map of the SAVMF showing location of the Coronation Hill and El
Sherana deposits and other U deposits. b) Map of Australia showing location of the (SAVMF)
in Northern Territories. c) Simplified map of Pine Creek Orogen, showing the Coronation
Hill and El Sherana deposits in the SAVMF, U deposits in the Alligator Rivers Uranium Field
(ARUF), and deposits in the Rum Jungle Mineral Field (RJMF) (modified from
www.ga.gov.au/minerals/projects/current projects/ geologica lmapsstandards.html).
In this chapter, we evaluate the character and formation of U mineralization of the El
Sherana and Coronation Hill deposits in the SAVMF, using a mineral paragenesis that
details the relative timing of alteration minerals in the deposits (Fig. 4.1). We also constrain
the timing, nature and origin of the fluids that produced and affected the deposits using
135

stable isotope geochemistry, U-Pb geochronology of paragenetically well-characterized U-
rich minerals, and chlorite and uraninite crystal chemistry. These results are used to identify
key processes controlling U mineralization in the SAVMF, present a genetic model for U
mineralization, and compare the South Alligator Valley U deposits to those in the younger
and U-rich Kombolgie Basin.
4.2. Geologic Setting
4.2.1. General geology
The South Alligator Valley area, Northern Territories, Australia (Fig. 4.1) comprises
rocks dated from Neoarchean to Paleoproterozoic, which are divided into four main
sequences. 1) Neoarchean basement granitic units (ca. 2.5 Ga; Needham and Stuart-Smith,
1985; Needham et al., 1988); 2) Paleoproterozoic sedimentary rocks of the Pine Creek
Orogen (2200 Ma to 1870 Ma) uncomformably overlying Neoarchean basement rocks
(Needham et al., 1987); 3) Paleoproterozoic silisiclastic red beds and associated volcanic
rocks of the El Sherana-Edith River Group (1829 Ma to 1822 Ma), which uncomformably
overlie Pine Creek Orogen sediments (Jagodzinski, 1992); and 4) late Paleoproterozoic
sedimentary rocks of the Kombolgie Basin (1822 Ma to 1720 Ma; Sweet et al., 1999)
uncomformably overlying older rocks and intruded by the 1723±6 Ma Oenpelli dolerite
(e.g. Kyser et al., 2000).
In the SAVMF, the oldest exposed unit of the Pine Creek Orogen sequence is the
Mundogie sandstone of the Mount Partridge Group (2025 Ma, Worden et al., 2004),
followed by the Koolpin Formation, the basal unit of the South Alligator Group (Needham,
1987). Sedimentation of the Koolpin Formation was accompanied by felsic volcanism,
136

epresented by the 1884±3 Ma Gerowie Tuff (Pietsch and Stuart-Smith, 1987) and the
overlying 1877±11 Ma Mount Bonnie Formation (Needham et al., 1988). These rocks are
uncomformably overlain by the ca. 1863 Ma Finniss Group (Walpole et al., 1968).
Following deposition of the Pine Creek Orogen sequence, the 1870±6 Ma Zamu
Dolerite sills (Page et al., 1980) were intruded, folded, and metamorphosed with the host
rocks by the 1860–1840 Ma Nimbuwah event of the Top End Orogen (Ferguson and
Needham, 1978; Lally and Worden 2004). In the SAVMF, the regional metamorphic grade
is greenschist facies (Needham et al., 1988a). Deformation and metamorphism were
accompanied and followed by emplacement of granitic rocks (Stuart-Smith et al., 1993;
Ferenczi and Sweet, 2005; Rasmussen et al., 2006; Neumann and Fraser, 2007).
Following exhumation of the final stages of the Nimbuwah event, minor deformation
and rift-related sedimentation occurred during the ca. 1825 Ma Cullen Event (Wyborn et
al., 1997), resulting in deposition of the El Sherana Group (Needham et al., 1988a). The El
Sherana Group consists of the Coronation sandstone and associated felsic volcanics, the Pul
Pul Rhyolite at 1829±5 Ma (Jagodzinski, 1991). Following folding, faulting and erosion of
the El Sherana Group, the Edith River Group (Kurrundie Sandstone) overlain by the Plum
Tree Creek volcanics at 1822±6 Ma (Jagodzinski, 1992) were deposited. Ahmad et al.,
(2006) interpreted the initial deposition of the El Sherana Group at 1865 Ma associated
with graben formation centred on the South Alligator River valley and followed later by
rifting and deposition of the Edith River Group at 1850 Ma. A regional low-grade
metamorphism, the ca. 1780 Ma Shoobridge event, may represent a thermal stage
137

coincident with the initiation of sedimentation in the McArthur Basin (Wyborn et al.,
1997).
All of these rocks are uncomformably overlain by the Paleoproterozoic fluvial redbed
sandstone successions of the Kombolgie Basin (Ojakangas, 1979; Sweet et al., 1999),
which is part of the McArthur Basin sequence (Kyser et al., 2000). Rocks of the Kombolgie
Basin were intruded by the late Paleoproterozoic 1723±6 Ma Oenpelli dolerite (e.g. Kyser
et al., 2000).
In the South Alligator Valley, the Pine Creek Orogen rocks were deformed during the
1870-1780 Ma Top End Orogen (Needham and DeRoss, 1990). Johnston (1984) and
Valenta (1990) identified three deformation phases. D 1 occurred during the 1890–1870 Ma
Barramundi Orogen (Page and Williams, 1988) and produced meso-scale isoclinal folding
and bedding-parallel cleavage, related to major low-angle reverse faulting, at the base of
the Koolpin Formation. D 2 occurred during the 1860-1840 Ma Nimbuwah tectonic event
and formed regional-scale, northwest trending, upright, tight to isoclinal folds, and a
penetrative axial-plane cleavage. Open, upright northeast-trending southeast-plunging folds
and fault movements formed during D 3 and affected the El Sherana and Edith River Group
rocks. (Valenta, 1991; Lally and Bajwah, 2006).
4.2.2. Uranium mineralization
Uranium deposits of the SAVMF are on or near the El Sherana–Palette fault system
(Fig. 4.1; Valenta, 1990), and were formed in dilatational zones at fault bends or
intersections (Valenta, 1991). The mineralization occurred as vein-type lodes in faults at the
unconformity between the El Sherana Group and the underlying Koolpin Formation
138

(Mernagh et al., 1994). Uraninite is associated with galena, chalcopyrite, pyrite, gold, and
clausthatite (Ayres et al., 1975). The alteration is dominated by quartz+sericite±chlorite±
kaolinite+hematite (Mernagh and Wyborn, 1994).
Mernagh et al. (1994) suggested that highly oxidizing, acid and low temperature
basinal brines transported Au–PGE–U as oxy-chloride and chloride species and proposed a
model for the Coronation Hill deposit wherein U mineralization formed by reaction of
acidic oxidized basinal brines from the cover sandstone with reducing basement rocks of
the Koolpin Formation. The precipitation of Au-PGE ore in the quartz feldspar porphyry
resulted from acid neutralization and moderate reduction from fluid interaction with
feldspathic host rocks (Mernagh et al., 1994). Ayres (1975) suggested that the U source was
the El Sherana Basin volcanics. The U-bearing groundwater percolated down to an aquifer
in the sandstone unit at the base of the volcanics. U precipitation occurred where U-bearing
basinal brines reacted with reducing carbonaceous shales of the Koolpin Formation.
Previous dating of uraninite from the SAVMF deposits proved inconclusive.
Uraninites from the El Sherana and Palette deposits have U-Pb ages ranging from 815 Ma
to 710 Ma (Hills and Richards, 1972; Cooper, 1973). Thermal Ionization Mass
Spectrometry (TIMS) dating of U-bearing samples indicate young 207 Pb/ 206 Pb ages ranging
between 830 Ma and 494 Ma and an U-Pb upper intercept of 730 Ma at the Palette deposit
whereas 207 Pb/ 206 Pb dates of 1196 Ma and U-Pb upper intercept ages of 1600 Ma occur at
the El Sherana deposit (Greenhalgh and Jeffery, 1959). U-Pb dating of uraninite from the
Palette deposit gives 207 Pb/ 206 Pb dates ranging from 964 Ma to 634 Ma (Greenhalgh and
Jeffery, 1959) and uraninite analyzed by laser ablation-high resolution inductively-coupled
139

plasma mass spectrometry (LA-HR-ICP-MS; Chipley et al., 2007) yielded 207 Pb/ 206 Pb dates
between 1855 Ma and 820 Ma at the El Sherana deposit and between 964 Ma and 634 Ma
at the Palette deposit (Chipley et al., 2007). Uraninite from the Adelaide River deposit
gives 207 Pb/ 206 Pb ages ranging between 1069 Ma and 735 Ma (Chipley et al., 2007). Ages
for the unconformity-related U deposits in the overlying Kombolgie Basin are 1675 to 1650
Ma (Polito et al., 2004; 2005).
4.3. Characteristics of selected uranium deposits
4.3.1. Coronation Hill uranium deposit
The oldest rocks in the Coronation Hill deposit area consist of interbedded
ferruginous slate, carbonate and quartzite of the Koolpin Formation and green
volcanoclastic sedimentary rocks (Fig. 4.2; Wyborn et al., 1991). Quartz-feldspar porphyry
and mafic intrusive rocks are correlated with the Gerowie Tuff (Carville et al., 1991) and
the Zamu Dolerite (Warren and Kamprad, 1990), respectively. The mafic intrusive rocks
consist of quartz diorite and minor granophyre, which are overlain by a sedimentary breccia
that is part of the Coronation sandstone (Mernagh et al. 1994). All of these rocks are
uncomformably overlain by a quartz sandstone unit of the Kombolgie Formation (Fig. 4.2,
Carville et al., 1991).
Valenta (1991) described three events of faulting. East-striking normal faults separate
quartz-feldspar porphyry and conglomerate and are overprinted by a north-striking dip-slip
fault that separates conglomerate and green volcanoclastic sedimentary rocks. North
northwest-striking, subvertical, strike-slip shear zones offset earlier faults and control the
mineralization (Mernagh and Wyborn, 1994; Eupene, 2003).
140

100m
Figure 4.2. (A) Geological plan of the Coronation Hill deposit showing main lithological units
and structural elements. (B) East-west geological cross-sections (line AB) across the
Coronation Hill deposit illustrating lithological units, fault systems and location of Au-PGE
and U-Au-PGE mineralization (modified from Wyborn et al., 1990).
141

The Coronation Hill deposit occupies a zone of complex faulting near the El Sherana-
Palette fault system (Fig. 4.1) and was mined between 1955 and 1964. Over this period,
25,306 metric tons of U ore grading 0.26% U 3 O 8 were mined (Fisher, 1969). Some gold
and PGE (4 850 000t at 4.31 g/t Au, 0.65 g/t Pd and 0.19 g/t Pt) were recovered from the
deposit. Two types of ore have been recognized (Fig. 4.2B). 1) U±Au mineralization in
faulted blocks of the Koolpin Formation (Needham, 1987), and 2) a Au-PGE±U orebody in
a north northwest-trending zone of fractured and sheared volcanoclastic rocks, quartzfeldspar
porphyry, sedimentary breccia and diorite (Carville et al., 1990, 1991).
4.3.2. El-Sherana uranium deposit
The El Sherana deposit is located within the El Sherana–Palette fault (Fig. 4.1;
Valenta, 1991). The deposit area consists of interlayered cherty ferruginous and
carbonaceous shale of the Koolpin Formation, uncomformably overlain by the Coronation
sandstone and volcanics of the Pul Pul Rhyolite (Fig. 4.3). The two dominant faults are
steeply southwest-dipping normal faults and younger, shallowly southwest-dipping reverse
faults (Valenta, 1991). Faulted and brecciated contact between carbonaceous and
ferruginous shale was the focus of the U mineralization (Fig. 4.3, Lally and Bajwah, 2006).
The uranium ore is hosted within subvertical, northwest-trending, interlayered cherty
ferruginous shale and carbonaceous shale at the unconformity below the Coronation
sandstone (Fig. 4.3; Crick et al., 1980). Minor mineralization also occurred within the
Coronation sandstone and altered volcanic rocks close to the unconformity.
142

Surface
100m
Figure 4.3. Geological cross-section of El Sherana and El Sherana West U deposits showing
main lithological units and location of the U mineralization. (modified from Valenta, 1991)
The mineralized zone has a strike length of 400 m and a vertical range of 180 m (Taylor,
1968). The total production was 226 t U 3 O 8 and 0.33 t Au from El Sherana, and 185 t U 3 O 8
and 0.007 t Au from El Sherana West during the period 1956-1964. Primary U
mineralization occurs as pods, lenticular masses, veins and disseminations and is associated
with fault zones and brittle fracturing (Taylor, 1968; Ayres and Eadington, 1975; Valenta,
1989, 1991). Gold occurs as veinlets within the uranium ore or as separate zones of
mineralization. Minor galena, angelsite, clausthalite, pyrite, marcasite, cobalt-nickel
143

arsenides, nickel selenide and copper sulfides are also associated with the ore (Threadgold,
1960).
4.4. Methodology
Polished thin sections were prepared from 250 core samples from the El Sherana and
Coronation Hill deposits (Fig. 4.1) and were examined using transmitted and reflected-light
microscopy to determine mineral crosscutting relationships and develop a paragenetic
succession for the area.
Electron microprobe analysis of syn-ore chlorite and uraninite were done on polished
thin sections using a JEOL JXA-8230 equipped with five wavelength dispersive
spectrometers (WDS) at Queen’s University, Canada. A suite of well-characterized natural
and synthetic minerals and compounds were used as calibration standards. Analytical
conditions were 15 kV accelerating voltage, 10 nA beam current, and a defocused beam.
Typical counting times were 10 s for major elements and 20 s for minor elements.
Analytical errors were

University, Canada. Monomineralic fractions, typically >95% pure, were used for stable
isotope analyses at the Queen’s Facility for Isotope Research. Oxygen isotopic
compositions of muscovite and kaolinite were measured using the BrF 5 method of Clayton
and Mayeda (1963) and a dual inlet Finnigan MAT252 isotope ratio mass spectrometer.
Hydrogen isotope compositions were determined using a Thermo Finnigan TC/EA in-line
with a DeltaPlus XP Finnigan Mat mass spectrometer. Isotopic compositions are reported
in the δ notation in units of permil (‰) relative to V-SMOW. Analyses of δ 18 O were
reproducible to ±0.2‰, and δ 2 H values were reproducible to ±3‰. The isotopic
composition of fluid was calculated using the oxygen isotope fractionation factors proposed
by O’Neil and Taylor (1969) for water-muscovite and Sheppard and Gilg (1996) for
kaolinite-water. The hydrogen isotope fractionation factors of Sheppard and Gilg (1996)
were used for water-muscovite and of Capuano (1992) for kaolinite-water.
U-Pb isotope ratios were determined by laser ablation-high resolution inductivelycoupled
plasma mass spectrometry (LA-HR-ICP-MS; Chipley et al., 2007) using a
Finnigan MAT Element 1 HR-ICP-MS and a Neptune HR-MC-ICP-MS, both equipped
with a high-performance Nd.YAG New Wave UP-213 laser ablation system at Queen's
Facility for Isotope Research. Ablation of uraninite was achieved on polished thin sections
using a 30 to 40μm spot size with 35% to 40% laser power at a frequency of 2Hz. The
argon gas flows were as follows; cooling gas, 1.5l/min; auxiliary gas, 1.0l/min; and sample
carrier gas, 1.0 l/min. A low resolution of 350 defined as the ratio of mass over peak width
mass at 5% of the signal height was used. For each sample, 204 Pb, 206 Pb, 207 Pb, 235 U, and
238 U were measured and corrections for common Pb were made scan-by-scan to each spot.
145

No corrections were made to the 238 U/ 235 U ratios as they were near the 137.8 natural ratios.
Instrument checks were done using an in-house uraninite standard.
Mineral name abbreviations used in this chapter are those from Kretz (1983). The
superscript numerical value on the mineral name abbreviations reflects the mineral growth
stages.
4.5. Results
4.5.1. Mineral Paragenesis
4.5.1.1. Coronation Hill uranium deposit
Mineral paragenesis for the Coronation Hill deposit is based on textural relationships
shown in Figures 4.4, 4.5, 4.6 and 4.7. Quartz-feldspar porphyry and granophyre rocks host
the U mineralization and three main stages of alteration: pre-ore, syn-ore, and post-ore
alteration. The quartz-feldspar porphyry is composed of Qtz 0 quartz and Kfs 0 feldspar
xenoliths of variable size embedded in a fine-grained matrix composed of Qtz 0 quartz, Kfs 0
feldspar, and Ms 0 muscovite (Fig. 4.5A). The granophyre rock consists of Qtz 0 quartz and
Kfs 0
alkali feldspar in characteristic angular intergrowths, embedded in a groundmass
consisting of fine-grained Qtz 0 quartz and Kfs 0 feldspars, Ms 0 muscovite and Bt 0 biotite
(Fig. 4.4).
4.5.1.1.1. Pre-ore alteration
Pre-ore alteration of the quartz-feldspar porphyry is characterized by fine-grained
Qtz 1 quartz grains as overgrowths on Qtz 0 quartz xenoliths (Fig. 4.5A). Src 1 sericite is the
most extensive alteration and occurs as fine-grained replacement of Qtz 0 quartz and Kfs 0
146

Deformation-Metamorphism:
1860-1840 Ma (Nimbawah Event)
Deposition of El Sherana Group (ca. 1830 Ma)
Deposition of Kombolgie Group (ca. 1750 Ma)
feldspar xenoliths in the matrix (Fig. 4.5A). In places, Kfs 0
feldspar xenoliths are
completely replaced by Src 1 .
Minerals
Deposition of Koolpin Formation and associated volcanic rocks (1900-1870 Ma)
Quartz Qtz 0
Feldspar KFs 0
Biotite* Bt 0
Muscovite Ms 0
Pre-Ore alteration
Quartz overgrowth Qtz 1
Sericite Src 1
Monazite Mzn 1
Titanite Tt 1
Chalcopyrite Cpy 1
Pyrite Py 1
Apatite* Ap 1
Early quartz vein Qtz 2 140 o C
Hematite Hem 1
Chlorite Chl 1 160 o C
Calcite Cal 1
Main U mineralization Event
250 o C
Chlorite Chl 2
Calcite Cal 2
Muscovite Ms 2
Uraninite U 1 1820Ma
Hematite Hem 2
Galena Pb 1
Gold Au 1
Chalcopyrite Cpy 2
Late alteration Event
Chlorite Chl 3 100 o C
Secondary uraninites U 2
Calcite Cal 3
Quartz Qtz 3
Hematite Hem 3
Azurite Az 1
Kaolinite Kln 1
Relative timing
Host rock
Pre-ore Syn-ore Post-ore
Figure 4.4. General mineral paragenesis of the Coronation Hill deposit. The three main
alteration stages include a pre-, syn-, and post-ore alteration of the basement rocks. The
thickness of the lines indicates the relative mineral abundance. An asterisk (*) marks the
primary minerals present in quartz feldspar porphyry and granophyre rocks. Temperatures
associated with the different alteration minerals are derived from their chlorite crystal
chemistry. The temperature of 140 o C for the pre-ore Qtz 2 is from Mernagh et al. (1994),
147

which was interpreted as being associated with the U mineralization. The age of 1820 Ma is
interpreted from U-Pb geochronology of paragenetically constrained U 1 . (See text for details).
Disseminated Cpy 1 chalcopyrite and Py 1 pyrite are present in the most altered
samples. Mzn 1 monazite associated with Ttn 1 titanite occurs as disseminated aggregates of
grains (Fig. 4.5B) and Ap 1 apatite occurs as elongated euhedral and transparent tabular
crystals (Fig. 4.5C). Early Qtz 2 quartz veins crosscut the quartz-feldspar porphyry (Fig.
4.5D) and occur locally as stockworks. Chl 1 chlorite is present as replacement of Src 1
sericite in the matrix (Fig. 4.5E) or frequently as coarse, felty-textured, radiating aggregates
coating Qtz 2 veins (Fig. 4.5D) where it forms thin needles crosscutting Qtz 2 veins (Fig.
4.5D). Hem 1 hematite forms primary inclusions in Qtz 2 veins where it replaces Chl 1
chlorite needles (Fig. 4.5D) and Src 1 sericite (Fig. 4.5E) in the matrix. Cal 1 calcite also
replaces Src 1 sericite and Chl 1 chlorite in the matrix (Fig. 4.5F).
The granophyre rock displays a similar pre-ore alteration pattern. Src 1
sericite
replaces Kfs 0 alkali feldspar in quartz-alkali feldspar intergrowths. Src 1 sericite is later
replaced by Cal 1 calcite. Bt 0 biotite and Ms 0 muscovite laths are typically pseudomorphous
after Chl 1 Chlorite. Ap 1 apatite, Hem 1 hematite and Ttn 1 titanite are part of the pre-ore
assemblage.
148

A
C
B
Qtz 0
Mzn 1
Qtz 0
Qtz 1 Ttn 1
Src 1
Cpy 1
Qtz 0 Hem 1
500μm
Chl 1
D
Ap 1 Qtz 2 Hem 1
Chl 1
500μm
150μm
Qtz 2
100μm
E
Cal 1 Src 1
Cal 1
Src 1 Hem 1 Chl 1
Chl 1
F
250μm
500μm
Figure 4.5. Photomicrographs of typical mineral alteration phases of the pre-ore stage. (A)
Pre-ore alteration of the quartz-feldspar porphyry showing fine-grained Qtz 1 overgrowth on
xenolith Qtz 0 . Src 1 occurs as fine-grained minerals replacing Qtz 0 and Kfs 0 into the matrix.
(B) Altered quartz-feldspar porphyry showing disseminated Cpy 1 , aggregates of Mzn 1
associated with Ttn 1 , Chl 1 and Hem 1 . (C) Quartz-feldspar porphyry matrix showing elongated
euhedral and transparent crystals of Ap 1 . (D) Early Qtz 2 vein crosscutting the quartz-feldspar
149

porphyry and coated by Chl 1 forming thin needles injecting into the Qtz 2 vein. Hem 1 occurs as
inclusions in Qtz 2 and as fine grains replacing Chl 1 needle. (E) Highly altered quartz-feldspar
porphyry showing Hem 1 and Chl 1 as replacement of Src 1 in the matrix. (F) Altered quartzfeldspar
porphyry showing Cal 1 as replacement of Src 1 in the matrix.
4.5.1.1.2. Uranium and gold mineralization
Following the pre-ore alteration stage, the host rocks of the Coronation Hill deposit
were brecciated and mineralized. Mineralization consists of U 1 uraninite, Au 1 gold and Gn 1
galena confined to zones that were mostly affected by the pre-ore alteration. Cross-cutting
relationships show that the ore assemblage crosscuts and obliterates the pre-ore mineral
assemblage. Mineralized breccias typically comprise sub-angular and altered quartzfeldspar
porphyry fragments cemented by U 1 uraninite (Fig. 4.6A) that occurs as massive
grains occupying open space in the matrix or as veins crosscutting the pre-ore assemblage
minerals.
U 1 uraninite is associated with Cal 2 calcite, Chl 2 chlorite, Hem 3 hematite (Fig. 4.6B),
and Ms 2 muscovite (Fig. 4.6C). In places, U 1 uraninite coats or replaces Py 1 pyrite grains
(Fig. 4.6D). U 1 uraninite is also disseminated in the granophyre, wherein it is associated
with Chl 2 chlorite, Cal 1 calcite, and Hem 2 hematite. U 1 uraninite is associated with the
assemblage Gn 1 Galena- Au 1 gold- Cpy 2 chalcopyrite (Fig. 4.6E). Gn 1 galena occurs as fine
white crystals, typically less than 50 μm across, or generally as massive euhedral to
anhedral grains greater than 1 mm in size.
Crystals of Gn 1 galena are intimately intergrown with U 1 uraninite, native Au 1 gold
and Cpy 2 chalcopyrite (Fig. 4.6E). Native Au 1 gold forms subhedral grains typically ca. 10–
150

100 μm diameter within Gn 1 galena (Figs. 4.6E and 4.6F). Cpy 2 chalcopyrite inclusions in
Gn 1 galena are common (Fig. 4.6E).
A
B
U 1 Cal 2
U 1
U 1 Chl 2
U 1
Altered quartz-feldspar
porphyry fragments
Hm 1
U 1
U 1 U 1
200μm
Src 1
150μm
C
D
U 1 Ms 1 U 1
Chl 1
Chl 2
Py 1
U 1
U 1 Qtz 1
100μm
500μm
E
U 1
U 1 U 2
U 1 U 2
U 2 Cpy 1
U 2 Gn 1
Au 1
Gn 1
Az 1 Au 1
Coffinite
Figure 4.6. Photomicrographs of typical mineral alteration phases of the syn-ore stage. (A)
151

Mineralized breccias showing quartz-feldspar porphyry fragments cemented by massive U 1 .
(B) Mineralized breccias showing U 1 vein crosscutting the early pre-ore alteration assemblage
and associated with Cal 2 , Chl 2 , and Hem 2 . (C) Syn-ore Ms 2 associated with the U 1 and Chl 1 .
(D) Mineralized breccias showing U 1 replacing early Py 1 grains. (E) Assemblage U 1 -Gn 1 -Au 1 -
Cpy 2 . Gn 1 galena as sub-euhedral crystals associated with native Au 1 , Cpy 2 and U 1 . Cpy 2 is
locally altered to Az 1 azurite. (F) Mineralized breccias showing U 1 intimately intergrown with
Gn 1 and Au 1 .
4.5.1.1.3. Post-ore alteration
Post-ore alteration is characterized by late mineralized veins containing banded
colloform U 2 uraninite coating Cal 3 calcite veins (Fig. 4.7A) and associated with minor
Chl 3 chlorite and Hem 3 hematite. U 2 uraninite fills late fractures indicating remobilization
during the post-ore alteration stage. Microprobe investigation reveals that secondary U 2
uraninite grains rim primary U 1 uraninite crystals in the ore (Figs. 4.6E and 4.6F). In
reflected light and backscattered electron images, U 2 uraninite is commonly heterogeneous
and zoned, has a mottled and speckled appearance, and forms sub -euhedral aggregates
(Fig. 4.6E). Post-ore Cal 4 calcite veins cut the ore assemblage (Fig. 4.7B). Thin, fibrous
Qtz 3 quartz veinlets crosscut the pre- and syn-ore assemblages (Fig. 4.7C). Cpy 2
chalcopyrite is locally altered to Az 1 azurite (Fig. 4.6E) likely during the post-ore stage.
Late Kln 1 kaolinite and Hem 4 hematite alteration obliterates earlier texture and minerals of
the pre-ore and syn-ore assemblage (Fig. 4.7D).
152

A
B
Cal 3 Cal 3
U 2 U 2 U 2 Cal 3 U 2
Sr 1 500μm Sr 1
Cl 1
500μm
C
D
S
U 1 Cpy 2
Qz 3 Kln 1
500μm
500μm
Figure 4.7. Photomicrographs of typical mineral alteration phases of the post-ore stage. (A)
Post-ore mineralized veins containing banded colloform secondary U 2 coating Cal 3 vein. (B)
Post-ore Cal 4 veins cutting the ore assemblage. (C) Thin, fibrous Qtz 2 veinlets crosscutting the
pre- and syn-ore assemblages. (D) Late Kln 1 obliterating earlier texture and minerals of the
pre-ore and syn-ore mineral assemblage.
4.5.1.2. El-Sherana uranium deposit
The mineral paragenesis for the El Sherana deposit is shown in Figures 4.8, 4.9 and
4.10. The basement Koolpin Formation rocks have been altered during pre-ore, syn-ore and
post-ore alteration stages while the overlying Coronation sandstone has been affected by a
pre-ore basin-related diagenetic alteration stage. The pre-ore alteration assemblage is absent
from the Coronation sandstone. This corroborates the suggestion of Wyborn et al. (1991)
153

SOUTH ALLIGATOR RIVER GROUP EL SHERAN GROUP
Coronation Sandstone
Koolpin Formationn
Deformation and Metamorphism 1860-1840 Ma (Nimbawah Event)
Deposition El Sherana Group (ca. 1830 Ma)..
that the pre-ore alteration formed during the Nimbuwah event that predates deposition of El
Sherana Group sediments.
Minerals Host rock Pre-ore Diagenesis Syn-ore Post-ore
Quartz Qtz 0
Feldspar KFs 0
Muscovite Ms 0
Tourmaline* Tur 0
Late events
Quartz overgrowth Qtz 2
Hematite Hem 3
Kaolinite Kln 1
Sericite Src 2
Calcite Cal 2
Monazite Mzn 1
Titanite Ttn 1
Secondary uraninite U 2
U n c o n f o r m i t y
Pre-ore alteration
Early quartz vein Qtz 1
Sericite Src 1
Chalcopyrite Cpy 1
Pyrite Py 1
Monazite Mzn 1
Titanite Ttn 1
Chlorite Chl 1 300 o C
Apatite Ap 1
Hematite Hem 1
Main U mineralization Event
Chlorite Chl 2 260 o C
Calcite Cal 1
Uraninite U 1 1820 Ma
Chalcopyrite Cpy 2
Galena Gn 1
Hematite Hem 2
Late events
Chlorite Chl 3
Hematite Hem 3
Kaolinite Kln 1
Secondary uraninite U 2 Relative timing
(B)
(A)
Figure 4.8. General mineral paragenesis of the El Sherana deposit for (A) basement rocks of
the Koolpin Formation and (B) Coronation sandstones of the El Sherana Group. The three
main alteration stages for the basement rocks include a pre-, syn-, and post-ore alteration.
The overlying Coronation sandstone is affected by diagenetic alteration, which postdates the
pre-ore alteration in the basement rocks. The thickness of the lines indicates the relative
mineral abundance. An asterik (*) marks the primary minerals present in the carbonaceous
shale and Coronation sandstones. Temperatures associated with the alteration minerals are
154

derived from their chlorite crystal chemistry. The age of 1820 Ma is interpreted from U-Pb
geochronology of paragenetically constrained U 1 .
4.5.1.2.1. Pre-ore basement hydrothermal alteration
The pre-ore alteration of the cherty ferruginous shale of the Koolpin Formation is
characterized by the occurrence of 0.1 to 1 cm-wide comb-textured Qtz 1 quartz veins (Fig.
4.9A). Crosscutting relationships indicate that Qtz 1
quartz veins predate massive
brecciation associated with pervasive Src 1 sericite alteration that fills and cements the pore
space between brecciated fragments (Fig. 4.9B). Src 1 sericite is replaced by Chl 1 chlorite
(Fig. 4.9C). Chl 1 chlorite also forms radially-textured laths around Qtz 1 quartz (Fig. 4.9D).
Their size and texture indicate growth into open pore spaces that were possibly created by
brittle deformation. Hem 1 hematite alteration is pervasive. The pre-ore assemblage includes
Ap 1 apatite (Fig. 4.9C), minor Mzn 1 monazite, Ttn 1 titanite, Cpy 1 chalcopyrite and Py 1
pyrite disseminated in the matrix in the most altered samples.
4.5.1.2.2. Pre-ore diagenetic alteration of the Coronation sandstone
Detrital minerals in well-sorted, quartz-dominated sandstones of the Coronation
sandstone consist of rounded Qtz 0 quartz grains and granite fragments (Fig. 4.10A), altered
Mzn 0 monazite (Fig. 4.10B), fragmented and altered Tur 1 tourmaline (Fig. 4.10C) and
altered Ms 0
muscovite laths (Fig. 4.10D). Diagenesis of the Coronation sandstone is
indicated by the occurrence of thin, discontinuous veneers of dark red-brown Hem 2
hematite (Fig. 4.10C) and well developed Qtz 2 quartz overgrowths that outline detrital Qtz 0
quartz grains (Fig. 4.10C).
155

A
Carbonaceous
Shale
B
Src 1
Qtz 1
Qtz 1
Qtz 1
500μm
Src 1 Qtz 1
Carbonaceous
Shale fragment
500μm
C
D
Src 1 Chl 2
Chl 1 Ap 1
Qtz 1
Chl 1
Src 1
500μm
E
Qtz 1
U 1
Qtz 1
Src 1 Src 1
Chl 1 Chl 2
Chl 1
Qtz 1 Cal 1
Cal 1
500μm
U 1
U 1
Src 1
F
Kln 2 Qtz 1
Cal 2
500μm
500μm
Figure 4.9. Microphotograph of typical mineral assemblages and crosscutting relationships of
the pre-, syn, and post-ore stage in the El Sherana deposit. A. Pre-ore Qtz 1 vein cutting the
interlayered cherty ferruginous shale of the Koolpin Formation. (B) Massive brecciation
associated with pervasive Src 1 alteration, which fills and cements the pore space between
brecciated fragments. (C) Pre-ore assemblage Src 1 replaced by Chl 1 . Chl 1 forms locally
radially-textured laths around Qtz 1 fragments associated with Ap 1 . (D) Syn-ore assemblage
156

cutting early Qtz 1 veins and the assemblage Src 1 -Chl 1 -dominated pre-ore alteration. (E) U 1
associated with Chl 2 , Cal 2 , and Hem 2 cutting the assemblage Src 1 -Chl 1 -dominated pre-ore
alteration. (F) Post-ore Kln 1 alteration obliterating texture of the pre-ore and syn-ore mineral
assemblage.
Qtz 2 quartz has Hem 3 hematite inclusions (Fig. 4.9C) and displays irregular contours
(Fig. 4.10C) that suggest partial dissolution during a late alteration event. Qtz 2 quartz
displays similar morphology to those recognized in sandstone of the Athabasca and
Kombolgie basins (Hiatt and Kyser. 2000; Polito et al., 2005; Hiatt et al., 2007). Pressure
solution features such as grain-point contacts and sutured grain boundaries are well
developed and locally forming stylolites. Kln 1 kaolinite alteration is pervasive and fills
well-developed secondary porosity (Fig. 4.10E) where it partially replaces detrital Ms 0
muscovite (Fig. 4.10D). The morphology of the Kln 1 kaolinite varies from coarse-grained
vermiform to very fine-grained (Fig. 4.10E). Aggregates of Ttn 1 titanite are disseminated
and generally associated with altered Mzn 0 monazite (Fig. 4.10B).
4.5.1.2.3. Uranium mineralization
The ore alteration stage in the basement overprints the pre-ore alteration assemblage.
Crosscutting relationships indicate that the syn-ore assemblage cross cuts Qtz 1 quartz veins
and the pre-ore alteration assemblage Src 1 sericite and Chl 1 chlorite (Fig. 4.9D). U 1
Uraninite is spatially associated with, or rimmed by Chl 2 chlorite, Cal 2 calcite, and Hem 3
hematite (Fig. 4.9E). Cpy 2 chalcopyrite and minor Gn 1 galena are associated with the U 1
uranium mineralization.
157

A
Granite
Qtz 0
fragments
Qtz 0
B
Mzn 1 Ttn 1 Qtz 0
Qtz 0 Kln 1
500μm
150μm
C
D
E
Kln 1 Kln 1
Qtz 0 Qtz 0
150μm
Kln 1
F
Qtz 0
Kln 1
Qtz 0 Src 2
Qtz 0 Kln 1 Qtz 0
250μm
Qtz 0 Hem 2 Qtz 0
Qtz 2 Tur 1
150μm
150μm
Figure 4.10. Photomicrographs of typical mineral assemblages of the Coronation sandstones.
(A) Well-sorted, quartz-dominated sandstones of the Coronation sandstone including rounded
Qtz 0 grains and granite fragments. (B) Altered Mzn 0 in sandstone. (C) Fragmented Tur 1 in
sandstone. Well-developed Qtz 2 overgrowths outlining detrital Qtz 0 grains in sandstone. Qtz 2
overgrowths have very fine Hem 2 grains inclusions and display irregular contours that
suggest partial dissolution during late alteration event. (D) Altered Ms 0 laths in the altered
158

sandstone. (E) Pervasive Kln 1 alteration in the sandstone filling well-developed secondary
porosity between detrital Qtz 0 grains. (F) Late Src 2 alteration replacing Kln 1 in sandstone.
The uranium mineralization was not observed in the overlying Coronation sandstone.
Ayres et al. (1975) observed minor uranium mineralization occurring within the Coronation
sandstone, close to the unconformity with the underlying mineralized Koolpin Formation.
4.5.1.2.4. Post-Ore alteration
Post-ore alteration in the basement rock is characterized by the occurrence of thin
veinlets of Chl 3 chlorite cutting through the syn-ore alteration assemblage. Late Kln 2
kaolinite alteration obliterates the pre-ore and syn-ore mineral assemblage (Fig. 4.9F).
Backscattered electron images indicate that U 1 uraninite is coarsely mottled and areas of
apparently pristine uraninite coexist with finely pitted altered U 2
uraninite. Post-ore
alteration in the Coronation sandstone is reflected also by the presence of minor Src 2
sericite that locally replaces Kln 1 kaolinite (Fig. 4.10F). Extensive secondary uranium
mineralization has been previously described associated with the overlying Coronation
sandstone (e.g. Valenta, 1991) (Fig. 4.3).
4.5.2. Crystal chemistry of the alteration minerals
4.5.2.1. Coronation Hill uranium deposit
4.5.2.1.1. Uraninite Crystal Chemistry
Electron microprobe analysis and backscatter images indicate that U 1 and U 2
uraninites have been variably altered to different forms of uranyl-silicates and have variable
U, Pb, Fe, Mg, Mn, and Ca contents (Table 4.1). These uraninites show considerable
variation in reflectance (Figs. 4.6E and 4.6F), suggesting significant heterogeneity in their
159

chemical composition as a result of alteration by later fluids (Kotzer and Kyser, 1993;
Polito et al., 2007). The chemical compositions of well-preserved U 1 uraninite (Table 4.1,
Sample C29-214B) have elevated amounts of PbO (4.5 wt% to 18 wt%) and UO 2 (71 wt%
to 85 wt%) and variable amounts of SiO 2 , CaO, FeO, Na 2 O, MnO, Y 2 O 3 , and P 2 O 5 . The
most reflective area in U 1 uraninite (Table 4.1, Sample C29-217A) has low silica contents
(e.g. from 0.4 wt% to 6.4 wt%) and high UO 2 contents (77 wt% to 86 wt %), in contrast,
the most altered area (U 2 ) have high silica contents (e.g. from 13.85 wt% to 21.88 wt%),
lower UO 2 contents (55 wt% to 65 wt%) and a low total due to the presence of structural
water (Table 4.1). The presence of these elements in the U structure reflects post-ore
alteration of the uraninite (Smith, 1984). U 1 uraninite has typically high P 2 O 5 (0.01 wt% to
1.64 wt%) and Y 2 O 3 (0.02 wt% to 5.52 wt%) contents (Table 4.1).
Sample I.D SiO 2 CaO FeO ThO 2 MnO UO 2 PbO Na 2O Y 2O 3 P 2O 5 Total
Chemical
Pb age
C29-214B-1 0.21 1.1 0.1 0.09 0.08 75.09 17.91 0.14 0.74 0.01 95 1479
C29-214B-2 0.62 1.7 0.2 0.23 0.16 79.91 10.65 0.19 0.44 0.04 94 827
C29-214B-3 1.22 3.33 0.36 0.12 0.35 81.56 6.8 0.25 0.62 0.07 95 517
C29-214B-4 1.19 2.86 0.35 0.2 0.33 83.46 5.21 0.23 0.73 0.07 95 387
C29-214B-5 0.36 1.34 0.17 0.04 0.11 77.7 16.21 0.1 0.32 0.04 96 1294
C29-214B-6 1.14 2.84 0.27 0.33 0.25 83.19 5.27 0.21 0.84 0.07 94 393
C29-214B-7 1.3 2.64 0.32 0.2 0.23 80.77 8.81 0.18 0.64 0.08 95 677
C29-214B-8 1.16 3.08 0.14 0.25 0.24 83.82 5.06 0.19 0.6 0.04 95 375
C29-214B-9 1.34 3.76 0.11 0.28 0.32 85.23 4.7 0.17 0.54 0.05 96 342
C29-214B-10 0.65 2 0.31 0.06 0.19 78.47 11.77 0.25 0.47 0.04 94 930
C29-214B-11 1.12 2.92 0.43 0.14 0.3 82.18 8.17 0.34 0.55 0.08 96 617
C29-214B-12 0.88 2.65 0.37 0.15 0.34 84.44 5.52 0.28 0.62 0.07 95 405
C29-214B-13 0.45 1.66 0.24 0.05 0.14 78.08 13.57 0.23 0.35 0.03 95 1078
C29-214B-14 1.04 2.74 0.37 0.25 0.29 82.62 6.54 0.28 0.63 0.06 95 491
C29-214B-15 1.34 3.54 0.46 0.24 0.44 83.18 4.57 0.27 0.78 0.08 95 341
C29-214B-16 0.87 2.16 0.21 0.13 0.18 78.39 11.57 0.18 0.45 0.06 94 916
C29-214B-17 1.76 3.88 0.13 0.26 0.29 83.36 4.55 0.16 0.47 0.06 95 338
C29-214B-18 0.44 2.3 0.19 0.04 0.16 81.12 10.77 0.21 0.44 0.03 96 824
C29-214B-19 0.85 2.53 0.28 0.21 0.21 80.49 9.25 0.19 0.47 0.05 95 713
C29-214B-20 0.37 1.39 0.17 0.04 0.1 75.38 14.93 0.19 0.46 0.03 93 1228
C29-214B-21 1.4 2.33 0.11 0.29 0.21 71.71 6.24 0.29 0.94 0.71 84 540
C29-217A-28 0.40 1.15 0.05 0.07 0.03 86.99 5.52 0.08 0.98 0.03 95 393
C29-217A-7 0.60 2.68 0.36 0.02 0.24 84.28 6.49 0.36 0.40 0.08 96 477
C29-217A-12 0.63 2.86 0.35 0.03 0.30 83.99 6.49 0.25 0.42 0.05 95 479
160

Sample I.D SiO 2 CaO FeO ThO 2 MnO UO 2 PbO Na 2O Y 2O 3 P 2O 5 Total
Chemical
Pb age
C29-217A-23 0.73 2.44 0.28 0.01 0.23 85.06 6.30 0.33 0.68 0.06 96 459
C29-217A-19 0.96 6.60 0.25 0.33 0.26 80.12 2.59 0.20 0.40 0.12 92 200
C29-217A-8 0.97 3.15 0.48 0.10 0.33 83.39 6.02 0.31 0.63 0.08 95 447
C29-217A-25 0.99 1.21 0.07 0.02 0.04 85.02 5.83 0.18 0.70 0.13 94 425
C29-217A-2 1.01 2.64 0.20 0.45 0.17 83.20 6.90 0.17 0.54 0.07 95 514
C29-217A-4 1.02 5.93 0.39 0.73 0.38 83.82 2.71 0.21 0.46 0.09 96 200
C29-217A-1 1.06 3.22 0.41 0.13 0.33 83.96 6.24 0.35 0.62 0.10 96 461
C29-217A-22 1.15 5.36 0.28 0.12 0.21 86.25 2.81 0.32 0.41 0.17 97 202
C29-217A-21 1.15 5.96 0.40 0.00 0.25 85.97 2.70 0.19 0.40 0.19 97 195
C29-217A-27 1.15 1.24 0.15 0.14 0.09 86.24 5.41 0.20 0.57 0.15 95 389
C29-217A-9 1.19 3.73 0.48 0.05 0.41 82.84 5.15 0.32 0.82 0.11 95 386
C29-217A-24 1.27 5.87 0.35 0.04 0.29 84.96 2.04 0.27 0.50 0.17 96 149
C29-217A-14 1.28 3.55 0.43 0.00 0.35 83.13 6.78 0.39 0.55 0.11 97 506
C29-217A-13 1.29 2.76 0.20 0.06 0.24 77.36 10.30 0.19 0.41 0.06 93 826
C29-217A-18 3.06 6.91 0.11 0.02 0.67 83.03 1.35 0.09 0.34 0.16 96 101
C29-217A-17 5.37 6.60 0.00 0.09 0.44 80.39 2.14 0.05 0.02 0.17 95 165
C29-217A-16 6.14 6.50 0.01 0.01 0.45 79.62 2.06 0.06 0.14 0.22 95 161
C29-217A-15 13.85 3.18 0.04 0.14 0.04 56.94 10.55 0.03 0.89 0.70 86 1150
C29-217A-11 13.98 3.27 0.00 0.18 0.05 55.03 5.28 0.04 2.16 0.95 81 595
C29-217A-6 15.68 3.53 0.02 0.07 0.12 62.37 0.44 0.03 4.12 1.43 88 43
C29-217A-3 16.33 3.12 0.01 0.03 0.05 59.01 4.35 0.02 4.29 1.64 89 458
C29-217A-5 16.80 3.74 0.00 0.00 0.09 65.86 0.65 0.05 2.14 0.97 90 61
C29-217A-26 18.50 3.30 0.01 0.00 0.00 61.86 0.27 0.02 5.52 1.45 91 27
C29-217A-29 18.58 3.20 0.01 0.00 0.01 61.92 0.07 0.01 5.09 1.27 90 7
C29-217A-20 21.88 3.33 0.01 0.01 0.08 59.86 0.58 0.02 1.94 1.03 89 60
C29-217B-1 0.92 2.83 0.27 0.04 0.26 83.72 6.28 0.24 0.71 0.08 95 466
C29-217B-2 1.03 3.23 0.19 0.03 0.29 80.04 9.41 0.18 0.50 0.07 95 729
C29-217B-3 1.17 3.21 0.23 0.04 0.27 82.90 5.95 0.23 0.61 0.07 95 445
C29-217B-4 4.13 6.78 0.05 0.02 0.65 82.47 2.83 0.07 0.39 0.08 97 213
C29-217B-5 0.99 2.82 0.23 0.03 0.24 84.64 6.33 0.24 0.57 0.07 96 464
C29-217B-6 4.67 8.00 0.00 0.00 0.58 78.29 2.99 0.06 0.53 0.11 95 237
C29-217B-7 0.48 2.72 0.30 0.03 0.27 85.76 5.72 0.25 0.57 0.07 96 414
C29-217B-8 4.51 5.58 0.02 0.00 0.38 81.05 2.19 0.15 0.75 0.26 95 168
C29-217B-9 4.12 7.33 0.11 0.00 0.69 81.89 0.50 0.09 0.75 0.20 96 38
C29-217B-10 4.36 6.20 0.10 0.00 0.49 82.51 0.70 0.15 0.76 0.26 96 52
C29-217B-11 0.54 2.43 0.29 0.02 0.26 85.80 5.76 0.31 0.73 0.08 96 416
C29-217B-12 0.56 2.04 0.23 0.00 0.19 85.75 6.33 0.26 0.54 0.07 96 458
C29-217B-13 1.54 3.74 0.20 0.00 0.34 83.80 4.60 0.17 0.64 0.09 95 340
C29-217B-14 1.11 2.82 0.19 0.01 0.23 84.04 6.09 0.26 0.57 0.10 95 449
C29-217B-15 1.53 3.26 0.16 0.03 0.27 83.52 5.58 0.18 0.52 0.09 95 415
C29-217B-16 1.12 3.33 0.35 0.01 0.34 82.58 7.10 0.25 0.69 0.10 96 534
C29-217B-17 0.67 2.44 0.24 0.00 0.23 83.59 7.03 0.25 0.67 0.07 95 522
C29-217B-18 1.22 3.60 0.36 0.02 0.30 82.56 6.22 0.37 0.79 0.11 96 468
C29-217B-19 1.11 3.32 0.33 0.01 0.33 83.84 4.96 0.27 0.78 0.12 95 367
C29-217B-20 0.60 3.76 0.16 0.08 0.16 86.48 3.64 0.25 0.77 0.11 96 261
C29-217B-21 8.49 0.00 0.00 0.02 0.28 72.01 4.44 0.22 0.83 0.40 87 382
C29-217B-22 18.58 3.49 0.02 0.00 0.01 63.53 0.34 0.03 3.61 1.45 91 34
C29-217B-23 19.34 3.25 0.01 0.04 0.04 61.61 0.38 0.01 3.80 1.15 90 38
C29-217B-24 0.89 5.07 0.17 0.01 0.18 82.87 2.86 0.38 0.66 0.17 93 214
C29-217B-25 0.94 5.68 0.25 0.00 0.18 82.83 2.69 0.28 0.77 0.28 94 201
C29-217B-26 0.96 5.37 0.25 0.00 0.19 86.27 2.92 0.34 0.72 0.20 97 210
C29-217B-27 1.09 2.93 0.27 0.06 0.26 83.12 5.44 0.26 0.62 0.11 94 406
161

Sample I.D SiO 2 CaO FeO ThO 2 MnO UO 2 PbO Na 2O Y 2O 3 P 2O 5 Total
Chemical
Pb age
C29-217B-28 1.03 2.96 0.25 0.06 0.25 83.60 5.66 0.24 0.64 0.10 95 420
C29-217B-29 0.44 2.35 0.27 0.06 0.25 84.03 6.28 0.34 0.62 0.07 95 464
C29-217B-30 0.50 2.19 0.25 0.03 0.21 82.86 5.60 0.32 0.80 0.09 93 419
C29-217B-31 2.65 4.91 0.10 0.02 0.58 81.79 3.84 0.12 0.56 0.08 95 291
Table 4.1. Results of the electron microprobe analyses for uraninite occurrences in the
Coronation Hill deposit with average chemical composition and calculated chemical Pb age.
The composition is reported in weight percent and the age in Ma.
4.5.2.1.2. Chlorite crystal chemistry
Pre-ore Chl 1
chlorite is Mg-rich with a calculated structural formula of
Mg 3.04 Al 2.53 Fe 0.47 (Si 3.3, Al 0.7 )O 10 (F 0.1 Cl 0.01 (OH) 7.89 ), corresponding to clinochlore (Deer et
al., 1992). Formation temperatures are near 160°C (Table 4.2), based on site occupancy
(Cathelineau, 1988). Syn-ore Chl 2 chlorite is similar in composition to pre-ore Chl 1 chlorite
with a structural formula of Mg 3.26 Al 2.52 Fe 0.89 (Si 3.03, Al 0.97 )O 10 (F 0.16 Cl 0.01 (OH) 7.73 , but with
formation temperatures near 250°C (Table 4.2). Post-ore Chl 3 chlorite has a structural
formula of Mg 2.67 Al 2.52 Fe 0.49 (Si 3.03 Al 0.97 )O 10 (F 0.16 Cl 0.01 (OH) 15.8 ) and records formation
temperatures near 100°C (Table 4.2). Chl 1 , Chl 2 and Chl 3 chlorites are low-Fe chlorite with
low Fe/Fe+Mg ratios (0.14 to 0.21) and high Si contents (Table 4.2), likely reflecting the
chemistry of the felsic quartz-feldspar porphyry host rock with which the hydrothermal
fluid has reacted. The composition of these chlorites includes trace amounts of Mn, F, and
Cl. Syn-ore Chl 2 chlorites have higher F contents (0.16 wt %; Table 4.2).
Coronation Hill Deposit
El Sherana Deposit
Pre-Ore Chl 1 Ore Stage Chl 2 Post-Ore Chl 3 Pre-Ore Chl 1 Ore Stage Chl 2
Oxides Wt % n=16 n=53 n=8 n=22 n=61
SiO2 33.48 30.76 35.64 26.11 28.44
TiO2 0.01 0.01 0.01 0.02 0.02
Al2O3 21.78 21.78 21.88 18.67 17.55
162

Coronation Hill Deposit
El Sherana Deposit
Pre-Ore Chl 1 Ore Stage Chl 2 Post-Ore Chl 3 Pre-Ore Chl 1 Ore Stage Chl 2
FeO 5.63 10.68 5.97 34.40 35.83
MnO 0.08 0.08 0.20 0.01 0.01
MgO 20.74 22.23 18.28 9.15 10.48
CaO 0.50 0.07 0.20 0.02 0.03
Na2O 0.05 0.02 0.05 0.02 0.02
K2O 0.40 0.05 0.72 0.03 0.02
F 0.25 0.39 0.23 0.13 0.16
Cl 0.05 0.03 0.04 0.01 0.02
H2O* 11.91 11.81 12.03 10.81 11.29
Total 94.87 97.93 95.23 99.38 103.86
Atomic proportion
Number of O 28.00 28.00 28.00 28.00 28.00
Tetrahedral sites
Si 3.30 3.03 3.49 2.86 2.98
Al iv 0.70 0.97 0.51 1.14 1.02
Total 4.00 4.00 4.00 4.00 4.00
Octahedral sites
Al vi 2.53 2.52 2.52 2.41 2.17
Ti 0.00 0.00 0.00 0.00 0.00
Fe2+ 0.47 0.89 0.49 3.15 3.14
Mn 0.01 0.01 0.02 0.00 0.00
Mg 3.04 3.26 2.67 1.50 1.64
Interlayers sites
Ca 0.05 0.01 0.02 0.00 0.00
Na 0.01 0.00 0.01 0.00 0.00
K 0.05 0.01 0.09 0.00 0.00
Total 0.11 0.02 0.12 0.01 0.01
Anions
O=F 0.10 0.16 0.10 0.06 0.07
0=Cl 0.01 0.01 0.01 0.00 0.01
OH* 15.67 15.51 15.70 15.81 15.78
Total 25.94 26.37 25.62 26.94 26.80
Fe/Fe+Mg 0.14 0.21 0.16 0.68 0.66
Temperatures o C 163 252 103 305 266
Table 4.2. Representative electron microprobe analyses of various chlorite phases from the
Coronation Hill and El Sherana deposits, including formation temperatures calculated using
the method of Cathelineau (1988). Calculated temperatures are accurate to 30°C based on
replicate analyses.
4.5.2.2. El-Sherana Uranium deposit
Pre-ore alteration Chl 1 chlorite is an Fe-chlorite with a calculated structural formula
of Fe 3.45 Mg 1.5 Al 2.41 (Si 2.86, Al 1.14 )O 10 (F 0.06 (OH) 7.94 ), reflecting the composition of chamosite
(Deer et al., 1992). Calculated formation temperatures are near 300°C (Table 4.2), based on
163

site occupancy (Cathelineau, 1988). Syn-ore chlorites Chl 2 are similar in composition to
pre-ore Chl 1 chlorites with a calculated structural formula of Fe 3.14 Mg 1.64 Al 2.17 (Si 2.98, Al 1.02 )
O 10 (F 0.07 Cl 0.01 (OH) 7.92 ). The calculated formation temperatures are near 260°C,
indistinguishable from those of the syn-ore chlorite from the Coronation Hill deposit. Chl 1
and Chl 2 chlorites contain lower MgO and higher FeO contents relative to those from the
Coronation Hill deposit (Table 4.2). They have high Fe/Fe+Mg ratios (0.66-0.68) and low
Si contents (Table 4.2) likely reflecting the chemistry of the host cherty ferruginous shale,
which has affected the mineralizing hydrothermal fluid. Syn-ore Chl 2 chlorites have trace
amounts of F (0.16 wt%) and Cl (0.02 wt%).
4.5.3. Isotopic compositions of minerals and fluids involved in the U mineralization
Pre-ore Src 1 sericite at the Coronation Hill deposit has δ 18 O values that range from
10.1 ‰ to 14.2 ‰ and δ 2 H values between -76 ‰ and -44 ‰ (Fig. 4.11; Table 4.3). Using
a formation temperature of 160°C based on coexisting chlorite (Table 4.2), Src 1 sericite
formed in equilibrium with a fluid having δ 18 O fluid values ranging from 5.1 ‰ to 7.7 ‰ and
δ 2 H fluid values from -84 ‰ and -52 ‰ (Fig. 4.11 ; Table 4.3 ). In contrast, pre-ore Src 1
sericite at the El Sherana deposit have higher δ 18 O values near 14.2 ‰ and δ 2 H values of -
44 ‰. With a formation temperature of 300°C (Table 4.2) the fluid that equilibrated with
the pre-ore Src 1 sericite at El Sherana has δ 18 O fluid and δ 2 H fluid values of 10.7 ‰ and -60‰,
respectively.
Syn-ore Ms 2 muscovite in textural equilibrium with U 1 uranium mineralization at the
Coronation Hill deposit has δ 18 O values that range from 11.8 ‰ to 13.8 ‰ and δ 2 H values
between -85 ‰ and -67 ‰ (Fig. 4.11; Table 4.3). Using a formation temperature of 250°C
164

calculated from chlorite crystal chemistry (Table 4.2), the calculated δ 18 O fluid and δ 2 H fluid
values for the mineralizing fluid that formed Ms 2 muscovite range from 2.8 ‰ to 4.8 ‰
and -75 ‰ to -57 ‰ respectively (Fig. 4.11; Table 4.3 ). At the El Sherana deposit the
isotopic composition of the mineralizing fluid is not obtainable due to difficulties from
separating pure syn-ore minerals.
Figure 4.11. Calculated δ 2 H and δ 18 O values of fluids in equilibrium with clay minerals from
various alteration stages of the basement rocks at the Coronation Hill and El Sherana deposits
(Table 4.3). Also shown are the meteoric water line and the isotopic composition of standard
modern ocean water (SMOW).
165

Mineral values Temperature Fluid values
Sample ID Deposits δ 18 O δ 2 H o C
δ 18 O fluid δ 2 H fluid
V-SMOW ‰ V-SMOW‰ V-SMOW‰ V-SMOW‰
Basement
Synore muscovite
C29-214 Coronation Hill 11.8 -74 250 2.8 -64
C29-195 Coronation Hill 13.8 -85 250 4.8 -75
C29-202 Coronation Hill 12.0 -67 250 3.0 -57
Pre-ore sericite
C29-189 Coronation Hill 12.7 -73 160 7.7 -81
C77-121 Coronation Hill 10.2 -53 160 5.2 -61
C29-209 Coronation Hill 12.7 -76 160 7.7 -84
C7788 Coronation Hill 11.8 -53 160 6.9 -62
C29-80 Coronation Hill 10.1 -44 160 5.1 -52
C29-80 (dup) Coronation Hill 10.1 -49 160 5.1 -57
E30-81 El Sherana 14.2 -44 300 10.7 -60
Table 4.3. Measured δ 18 O and δ 2 H for muscovite and calculated δ 18 O and δ 2 H values for fluids
in equilibrium with minerals from various alteration stages of the basement rocks at the
Coronation Hill and El Sherana deposits. Temperatures used to calculate the fluid values are
derived from the chlorite crystal chemistry (see Table 4.2)
4.5.4. Geochronology of uraninite and isotopic systematics
Paragenetically constrained uraninite from the Coronation Hill and El Sherana
deposits were dated by LA-HR-ICP-MS (Chipley et al., 2007). Uraninite samples analyzed
have a mottled appearance with micron-size areas that are highly reflective surrounded by
dull areas, which is typical of the ore from both deposits (Figs. 4.6E and 4.6F). The
majority of the U–Pb isotope ratios are significantly discordant, as in other deposits (e.g.
Fayek and Kyser, 1997; Polito et al., 2004). The oldest 207 Pb/ 206 Pb ages are likely to be
closer to the initial formation age because Pb-Pb ratios in U are less susceptible to resetting
by younger fluid events than are the U-Pb ratios (Collins et al., 1954). The errors observed
166

in the U-Pb systems are in large part a function of the U age (Chipley et al., 2007); older
uraninite is more likely affected by multiple alteration events so that errors obtained in the
U-Pb system are greater. Analytical results are presented in Table 4.4 and the U-Pb
concordia results summarized in Table 4.5.
4.5.4.1. U-Pb geochronology of U-rich minerals by LA-HR-ICP-MS
U 1 uraninite grains from the syn-ore stage at the Coronation Hill deposit have U-Pb
isotopic compositions that define a discordia line with an upper intercept age of 1823±140
Ma and an oldest 207 Pb/ 206 Pb age of 1719±31 Ma (2σ, MSWD=2.6) (Fig. 4.12A). Two
samples from the El Sherana deposit have upper intercept ages of 1819±150 Ma (2σ,
MSWD=7.8; Fig. 4.12B) and 1616±100 Ma (2σ, MSWD=1.02; Fig. 4.12C) and the oldest
207 Pb/ 206 Pb ages of 1810±15 Ma and 1825±90 Ma, respectively. The upper intercept and
oldest 207 Pb/ 206 Pb ages at Coronation Hill are identical to oldest 207 Pb/ 206 Pb ages at El
Sherana and can therefore be interpreted as the estimate formation age for U 1
mineralization.
The U-Pb system in uraninite from various samples from the Coronation Hill deposit
records various periods of post-mineralization alteration coincident with major tectonic
events that have affected the area. These ages include 1654±170 Ma and 1638±160 Ma
(Figs. 4.12D and 4.12E respectively), 1510±10 Ma (Fig. 4.12F), 1266±68 Ma (Fig. 4.12G),
and 837±130 Ma (Fig. 4.12H). Similar post-formation alteration dates of uraninite have
been reported from unconformity-type deposits in the Athabasca (Kotzer and Kyser 1993;
Fayek and Kyser 1997; Cloutier et al., 2009) and Kombolgie basins (Polito et al., 2004).
167

Corrected ratios
Apparent ages ( ±2σ, Ma)
Sample I.D Deposit n
206 Pb/ 204 Pb
207 Pb/ 204 Pb
207 Pb/ 206 Pb ±2σ
206 Pb/ 238 U ±2σ
207 Pb/ 235 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
c29-217 Coronation Hill 17 6022 420 0.0703 0.0009 0.1013 0.0042 0.9859 0.0391 0.90 935 27 622 24 695 20 26
C29-214 Coronation Hill 14 21973 1802 0.0813 0.0007 0.0886 0.0038 1.0014 0.0455 0.92 1224 18 545 23 692 23 56
C29-295 Coronation Hill 12 4045 238 0.0609 0.0016 0.0518 0.0060 0.4426 0.0522 0.90 619 56 322 36 349 33 46
C29-217Ac Coronation Hill 10 6216 516 0.0799 0.0012 0.1055 0.0063 1.1987 0.0760 0.90 1188 30 645 37 786 34 46
C29-217Ax Coronation Hill 11 6052 430 0.0706 0.0009 0.1028 0.0049 1.0044 0.0479 0.92 944 25 630 29 704 24 33
Cor29_201.6G Coronation Hill 18 1989 170 0.0885 - 0.1204 - 1.4988 - - 1387 39 742 57 911 58 -
El Sherana 7b El Sherana 14 - - 0.0936 - 0.0751 - 1.1023 - - 1492 - 463 - 729 - -
El Sherana 20 El Sherana 14 1823 - 0.0931 0.0034 0.0787 0.0045 0.9425 0.0351 0.32 1481 65 487 27 666 16 67
Table 4.4. Isotopic data of the U-Pb LA-HR-ICP-MS analysis and apparent-ages for uraninite from the Coronation Hill and El
Sherana deposits. The paragenesis of each type of uraninite analyzed is shown in Figures 4.3 and 4.5 and described in Section
4.2.1.1., R. error correlation coefficient, Disc‡. % discordant. n:number of grains. 206 Pb/ 238 U, 207 Pb/ 235 U, and 207 Pb/ 206 Pb ages are
calculated using equations reported by Ludwig (2000) and expressed in Ma.
168

A
B
C
D
E
F
169

G
H
Figure 4.12. U-Pb concordia diagrams from in situ isotopic analysis by LA-HR-ICP-MS of U-
rich minerals from the Coronation Hill and El Sherana deposits (see text for details).
Mineralization
event
Deposit
Upper
intercept age
(Ma)
Lower
intercept
age (Ma)
207 Pb/ 206 Pb
age (Ma)
MSWD
Figures
a. Primary uranium mineralization.
Coronation Hill 1823±140 362±82 1719±31 2.6 4.10A
El Sherana 1819±150 45±92 1810 7.8 4.10B
El Sherana 1616±100 160±49 1825 1.02 4.10C
b. Post-mineralization alteration events recorded in altered uraninite
Coronation Hill 1654±170 493±35 1169 1 4.10D
Coronation Hill 1638±160 486±32 1152 1.6 4.10E
Coronation Hill 1510±100 257±71 1402 3.8 4.10F
Coronation Hill 1266±68 23±73 1303 2.5 4.10G
Coronation Hill 837±130 122±90 1021 8 4.10H
Table 4.5. Summary of the U-Pb concordia results of U-rich minerals for various events of. a)
primary uranium mineralization and b) post-mineralization alteration event in the
Coronation Hill and El Sherana deposits.
170

4.5.4.2. Pb-Pb geochronology of galena and uraninite by LA-HR-ICP-MS
The Gn 1 Galena- Au 1 gold- U 1 uraninite assemblage from the Coronation Hill deposit
has been dated by means of Pb-Pb dating of cogenetic Gn 1 galena (Table 4.6). A Pb-Pb
isochron from Gn 1 galena in equilibrium with Au 1 gold and U 1 yields an age of 1601±98
Ma (Fig. 4.13A) recording a period of post-ore alteration coincident with the timing of
unconformity-related U mineralization in the Kombolgie Basin (Gulson and Mizon, 1980;
Page et al., 1980; Maas, 1989; Polito et al., 2004). This event is also identical to alteration
periods recorded in the U-Pb system in U 1 uraninite (Figs. 4.12D, 4.12C and 4.12E).
The Pb-Pb system in uraninite from various samples records periods of postmineralization
alteration events as well. Model ages obtained are 1412±86 Ma (Fig. 4.13B),
1282±54 Ma (Fig. 4.13C), 790±240 Ma (Fig. 4.13D), 719±110 Ma (Fig. 4.13E), and
377±67 Ma (Fig. 4.13F).
171

Figure 4.13. Pb-Pb isochron diagrams of galena and uraninite from the Coronation Hill
deposit.
Corrected ratios
Sample
206 Pb/ 204 Pb ±2σ
207 Pb/ 204 Pb ±2σ
207 Pb/ 206 Pb ±2σ
238 U/ 235 U ±2σ
238 U ±2σ
C29-217BPPz1 240.47 15.10 39.36 3.43 0.16 0.004 138 10.32 0.04 0.04
C29-217BPPz6 235.20 10.20 38.02 0.93 0.16 0.004 141 0.84 0.75 0.40
C29-217BPPz4 382.59 41.87 51.10 4.81 0.13 0.007 140 9.41 0.05 0.03
C29-217BPPz3 314.68 25.13 45.96 4.79 0.14 0.008 142 20.44 0.05 0.07
C29-217BPPz2 250.33 23.84 41.60 5.87 0.17 0.007 133 14.17 0.03 0.02
C29-217BPPy 227.09 8.98 38.43 2.50 0.17 0.005 135 7.67 0.17 0.18
C29-217BPPx 230.35 22.68 37.77 5.65 0.16 0.008 142 16.12 0.04 0.04
C29-217BPPw 266.64 25.05 40.11 4.33 0.15 0.005 145 13.02 0.05 0.04
C29-217BPPv 426.15 49.45 54.95 4.24 0.13 0.007 139 2.85 0.15 0.06
C29-217BPPu 294.97 10.66 43.59 1.68 0.15 0.003 140 4.47 0.07 0.05
C29-217BPPt 419.20 20.21 54.79 2.45 0.13 0.003 139 6.64 0.22 0.15
C29-217APPs 252.77 10.49 39.75 1.18 0.16 0.004 141 2.26 0.18 0.13
172

C29-217APPr 295.26 13.37 43.50 1.34 0.15 0.005 139 2.11 0.36 0.28
C29-217APPr1 246.05 19.17 39.12 1.72 0.16 0.006 140 1.97 0.21 0.09
C29-217APPq 242.05 24.61 38.84 5.90 0.16 0.009 143 18.50 0.02 0.01
C29-217APPp 195.35 1.13 32.74 0.53 0.17 0.000 154 2.72 0.02 0.01
C29-217APPo 224.24 53.26 38.51 12.99 0.17 0.021 157 61.47 0.02 0.02
C29-217APPm 236.15 7.59 38.67 1.01 0.16 0.005 139 2.80 0.19 0.11
C29-217APPk 211.22 9.58 36.70 2.11 0.17 0.003 142 7.34 0.07 0.04
C29-217APPh 644.46 57.38 81.54 10.87 0.13 0.006 116 15.61 0.07 0.00
C29-217APPg 187.96 16.40 34.21 3.95 0.18 0.009 145 22.67 0.02 0.01
C29-217APPf 247.09 18.16 40.02 4.70 0.16 0.007 145 16.59 0.01 0.00
C29-217APPd 233.28 9.80 38.43 2.41 0.16 0.006 139 7.35 0.08 0.05
Table 4.6. Isotopic analyses data of the Pb-Pb LA-HR-ICP-MS analysis of galena from the
Coronation Hill deposit. Result of the age model is shown in Figure 4.12A.
4.5.4.3. Chemical Pb age of the uranium mineralization
The chemical Pb age is derived from the assumption that the total Pb present in the
sample is of radiogenic origin, resulting exclusively from the decay of U and Th and that
the mineral has not lost or acquired Pb since it formed (Bowles, 1990). Different Chemical
Pb ages in the same grain reflect variable alteration by subsequent fluids during
recrystallization of the uraninite to new uranium minerals, resulting in a decrease in the
Chemical Pb age and an increase in elements other than uranium. As alteration is expected
to result in a decrease in radiogenic Pb contents, the formation age of the uraninite can be
estimated by extrapolating the Chemical Pb ages to when the concentrations of the
secondary elements (e.g. Ca, Fe and Si) were negligible (e.g. Alexandre and Kyser, 2005).
Chemical Pb ages derived from the composition of U 1 uraninite vary from 341 Ma to
1479 Ma (Table 4.1), suggesting variable recrystallization, Pb loss, and gain of elements
that make up new uranium alteration phases. Regression of the SiO 2 +Fe 2 O 3 +CaO+MnO
contents to zero in U 1 uraninite corresponds to 1822 Ma (Fig. 4.14), which is within error
identical to the U-Pb upper intercept dates of 1823±140 Ma and 1819±150 Ma (Figs. 4.12A
173

and 4.12B), and to 207 Pb/ 206 Pb ages of 1810±15 Ma and 1825±90 Ma (Figs. 4.12B and
4.12C).
Chemical Pb ages (Ma)
Figure 4.14. Plot of element contents in uraninite as a function of chemical Pb ages.
4.6. Discussion
Paragenetic minerals and geochronologic data from the Coronation Hill and El
Sherana deposits indicate that basement rocks of the Koolpin Formation and the overlying
El Sherana Basin sandstones have been affected by multistage deformation and fluid
events, including early stages of basement metamorphism and basin diagenesis followed by
hydrothermal alteration and U mineralization and post-ore alteration (Fig. 4.15, Table 4.7).
Alteration assemblage
Pre-ore Stage Diagenesis Ore Stage Post-ore stage
Src 1 -Chl 1 -Hem 1 -
Qtz 1 Kln1 -Hem 2 -Qtz 2 U 1 -Au 1 -Gn 1 -Chl 4 -
Cal 4 -Hem 4 U 2 -Chl 5 -Cal 5 -Hem 5
Age of formation 1860 – 1840 Ma 1830 – 1820 Ma 1820 Ma Post 1820 Ma
174

Tectonic Event
Formation
temperature
Pre-ore Stage Diagenesis Ore Stage Post-ore stage
Nimbuwah event
Late stage
Nimbuwah event
Post stage
Nimbuwah event
Various tectonic events
160 o to 300 o C - 250 o C ca. 100 o C
δ 18 O fluid (‰) 5.1 to10.7 - 2.8 to 4.8 -
δ 2 H fluid (‰) -81 to -52 - -75 to -57 -
Complexing agent F - , PO 3 -4 , Cl -
Fluid source
low grade
greenschist
metamorphic
Basinal Basinal Meteoric
Table 4.7. Summary of the major results presented in this chapter showing the paragenetic
mineral assemblages and timing of the U mineralization, major thermotectonic events,
formation temperatures, isotopic compositions of fluids, source of fluid events recorded in U
deposits in the SAVMF area. (Ap=apatite, Cal=calcite, Chl=chlorite, Hem=hematite,
Qtz=quartz, Src=sericite, U=uraninite).
4.6.1. Basement metamorphism and basin diagenesis
The pre-ore alteration assemblage Src 1 -Qtz 1 -Chl 1 -Cal 1
(Figs. 4.5 and 4.9) at the
Coronation Hill and El Sherana deposits is similar to alteration patterns described by
Warren and Kamprad (1990) and Wyborn et al. (1991), which they interpreted as related to
early metamorphism and metasomatism of the basement rocks during D 2 deformation
associated with the 1860-1840 Ma Nimbuwah tectonic event. This event predates
deposition of the ca. 1830 Ma El Sherana Group. δ 18 O and δ 2 H isotopic compositions of the
pre-ore Src 1 sericite indicate that the pre-ore alteration fluids at the Coronation Hill and El
Sherana deposits are metamorphic in origin (Fig. 4.11) and therefore associated with
deformation and regional metamorphism during the Nimbuwah event (Fig. 4.15 A). The
high δ 18 O value of pre-ore Src 1 sericite at the El Sherana deposit is indicative of extensive
water/rock interaction. The fluid formed at ca. 300 o C at the El Sherana deposit and ca.
175

160 o C at Coronation Hill. The temperature of ca. 300 o C at the El Sherana deposit is
consistent with fluids derived from low grade greenschist metamorphic processes (Wyborn
et al., 1991). Extensive hematite inclusions in pre-ore Qtz 2 quartz veins (Fig. 4.5D) at the
Coronation Hill deposit suggest that pre-ore metamorphic fluids were highly oxidized (e.g.
Mernagh et al., 1994).
A Sensitive High Resolution Ion Microprobe (SHRIMP) U-Pb age of 1827±3 Ma for
the Pul Pul Rhyolite (Jagodzinski, 1998) near the top of the El Sherana Group indicates that
sediments of the El Sherana Basin could have begun to accumulate well before ca. 1830
Ma during deformation associated with the Nimbuwah event (Fig. 4.15B). Ahmad et al.
(2006) suggested that the initial deposition of El Sherana Group sediments occurred at
around ca. 1865 Ma associated with graben formation centred on the South Alligator River
valley. Therefore deposition of the El Sherana Basin sediments took place rapidly in a
tectonically active environment associated with the Nimbuwah Orogen (Friedmann and
Grotzinger, 1994). The prevailing geothermal gradient must have been higher compared to
the younger and larger Kombolgie Basin.
Petrographic analysis of the Coronation sandstone at the El Sherana deposit indicate
features typical for diagenetic alteration processes (Fig. 4.10), including well developed
Qtz 2 quartz overgrowths outlining detrital Qtz 0 quartz grains accompanied by partial to
complete resorption and pressure solution features that occurred during compaction at deep
burial levels. Extensive Kln 1 kaolinite alteration that is associated with development of
secondary porosity indicates that there were diagenetic aquifers in the El Sherana Basin
sandstone, which could have conducted U-bearing basinal brines (Fig. 4.15B). This
176

alteration is similar to sandstone alteration of Proterozoic basins in Canada and Australia
(Wilson and Kyser, 1987; Kotzer and Kyser, 1995; Hiatt et al., 2001; Polito et al., 2005).
Koolpin Formation
Carbonaceous Shale
Koolpin Formation
Carbonaceous Shale
177

Figure 4.15. Conceptual genetic model for U mineralization in the SAVMF. A. Deformation,
metamorphism and metasomatism of the basement lithologies during the 1860-1840 Ma
Nimbuwah tectonic event. The pre-ore alteration Src 1 -Qtz 1 -Chl 1 -Cal 1
formed from
metamorphic fluids between 150 o and 300 o C. B. Deposition of the El Sherana Group during
extensional tectonism associated with the Nimbuwah event is followed by basin-diagenesis
during burial. Subsequently, reactivation of the El Sherana-Palette fault system more focused
in zones of pre-existing tectonic weakness that were previously affected by an early pre-ore
alteration, created structural traps for fluid flow, hydrothermal alteration and U
mineralization. The ore-forming fluids originated in the El Sherana Basin and descended
downward into the basement rocks along fracture systems. Interaction of the oxidizing
basinal brine with reducing lithologies of the Koolpin Formation led to deposition of the ore
metals at ca. 1820 Ma. C. U 1 was altered during multiple stages of fluid overprinting related
to fault reactivation during successive regional thermotectonic events that occurred over a
period of at least 1.8 Gyrs. These alteration events resulted in subsequent alteration of the
deposits and the formation of the post-ore mineral assemblage including widespread
secondary uraninite occurring as fracture-filling veinlets.
Koolpin Formation
Carbonaceous Shale
178

4.6.2. Hydrothermal alteration and uranium mineralization
Following metamorphism and pre-ore alteration of the basement and diagenesis of
the overlying Coronation sandstone of the El Sherana Basin, the rocks were affected by the
main U mineralization event associated with an intense brecciation that is likely related to
tectonic reactivation along the El Sherana-Palette fault system (Lally and Bajwah, 2006).
Petrographic and textural observations indicate a spatial relationship between the intensity
of the pre-ore alteration and the location of the U mineralization. Fault reactivation was
likely more focused in zones of pre-existing tectonic weakness that were previously
affected by pre-ore alteration, creating structural traps that were open for fluid flow,
hydrothermal alteration, and uranium mineralization. Syn-ore Ms 2 muscovite has δ 18 O and
δ 2 H isotopic compositions typical of low latitude basinal brines (Fig. 4.11) similar to those
of unconformity-related U-deposits in the Athabasca (e.g. Fayek and Kyser, 1997; Cuney
and Kyser, 2008) and Kombolgie basins (e.g. Polito et al., 2004, 2006). The ore-forming
fluid most likely originated in the El Sherana Basin and descended downward into the
basement rocks along fracture systems created by brittle reactivation of the El Sherana-
Palette fault system (Fig. 4.15B). The mineralizing brine contained U, Au and PGE, the
former most likely leached from detrital U-bearing minerals (e.g. monazite and apatite) in
the El Sherana Basin sandstone, and the Au and PGE from alteration of felsic volcanics and
mafic rocks that comprised much of the El Sherana Group subsequent to burial and
diagenesis (Fig. 4.15B).
The syn-ore alteration is associated with precipitation of U 1 ±Au 1 mineralization in
faulted and brecciated contact between reducing carbonaceous and cherty ferruginous shale
179

of the Koolpin Formation, while deposition of ±U 1 -Au 1 -PGE occurred in fractured and
sheared quartz-feldspar porphyry at the Coronation Hill deposit. The U 1 -Gn 1 -Au 1 -Cpy 2 ore
assemblage formed at temperatures of ca. 250 o C, based on chlorite crystal chemistry (Table
4.4, Cathelineau, 1988). Mernagh et al. (1994) indicated a temperature of 140 o C based on a
microthermometry study of quartz veins at Coronation Hill. However, cross-cutting
relations indicate that these quartz veins formed earlier, during the pre-ore alteration stage
and therefore, pre-date the U mineralizing event. Chl 2
chlorites at Coronation Hill
paragenetically associated with the Qtz 2 quartz veins have formation temperatures near
160 o C (Table 4.4), similar to temperatures proposed by Mernagh et al. (1994).
The presence of small amounts of fluorine and chlorine in syn-ore Chl 2 chlorite
(Table 4.4) and phosphate in U 1 uraninite (Table 4.1) suggest that fluorine, chlorine, and
phosphate were important ore transporting complexes. Uranium is mobile under oxidizing
conditions (Cuney and Kyser, 2008) and in oxidized aqueous basinal brines between pH 4
and 7.5, uranyl-phosphate complexes are the important species (Cuney and Kyser, 2008),
while chlorine- and fluorine-complexes are dominant in fluids under acidic conditions at
temperatures up to 200°C (Romberger, 1984; Kojima et al., 1994). Interaction of oxidizing
mineralizing fluid with the reducing Fe-rich interlayered cherty ferruginous shale of the
Koolpin Formation may have led to deposition of the U-ore metals at El Sherana.
Petrographic observation indicates that early Py 1 pyrite (Fig. 4.6D) in the basement rock
was a reductant so that Fe 2+ or S in Py 1 pyrite would have acted as reductants for U 6+ .
In hydrothermal fluids, Au and PGE are soluble as chloride complexes (Mountain
and Wood, 1988a, 1988b), which are more important in oxidized, low-temperature, acidic,
180

and saline fluids (Mernagh et al., 1994). Therefore, the occurrence of Au 1 -PGE±U 1
associated with the quartz feldspar porphyry at the Coronation Hill deposit may have
resulted from acid neutralization and moderate reduction resulting from fluid interaction
with feldspathic host rocks (Wyborn, 1992; Mernagh et al., 1994). Ore metal deposition is
therefore, strongly controlled by the composition of the host lithology (e.g. Needham and
Stuart-Smith, 1984; Needham, 1988b)
Our results corroborate Ayres (1975) suggestion that the Au source was the El
Sherana Basin volcanics, particularly the Pul Pul Rhyolite of the Coronation sandstone.
Mernagh et al. (1994) indicated that highly oxidizing, basinal, low temperature and low-pH
solutions transported simultaneously Au, PGE and U as oxy-chloride and chloride species,
but proposed the Kombolgie Basin sediments as the source of the mineralizing fluids. Sener
et al. (2002) suggested that the nature of the ore elements and alteration at the Coronation
Hill deposit is consistent with deposition from acid and oxidizing fluids.
Au and PGE are found in ore grade concentrations in unconformity-related uranium
deposits. For example, U ore in the Jabiluka deposit contains Au grading 10 g/t and
significant concentrations of Pd (Wilde et al., 1989). Unconformity-related U deposits in
the Athabasca Basin in Canada have also been reported to contain minor concentrations of
Au and PGE (Wray et al., 1985).
LA-HR-ICPMS data indicate that initial U precipitation occurred in the basement at
ca. 1820 Ma (Figs. 4.12A to 4.12C). The 1822 Ma chemical Pb age of U 1 uraninite (Fig.
4.14) at Coronation Hill is identical to the U-Pb concordia ages at the El Sherana deposit
(Figs. 4.12A to 4.12C). These ages suggest that the U mineralization in the SAVMF formed
181

at ca. 1820 Ma, approximately 40 Myr after initial deposition and diagenesis of the EL
Sherana Basin.
The timing of the U-Au-PGE mineralization at the Coronation Hill at El Sherana
deposits is coincident with a period of regional extension tectonism and granite intrusion in
the Pine Creek Orogen (Ferguson et al., 1980a; Stuart-Smith and Needham, 1984;
Needham et al., 1988). These granites include the 1820±8 Ma Malone Creek Granite
(Edgecombe et al., 2002), which intruded El Sherana Group rocks, the ca. 1820 Ma
calcalkaline Cullen Suite granite intruding the Pine Creek Orogen (Stuart-Smith et al.,
1993) and the 1818±3 Ma Fenton Granite in the Gold Ridge area (Needham et al., 1988).
4.6.3. Late stage alteration and resetting events
Post-ore alteration recorded in uraninite samples indicate that the U-Pb and Pb-Pb
isotopic system in U 1 uraninite and cogenetic Gn 1 galena were reset during multiple fluid
events related to fault reactivation during successive regional thermotectonic events that
occurred over a period of at least 1.8 Gyrs (Figs. 4.15A and 4.16). These alteration events
resulted in subsequent alteration of the El Sherana and Coronation Hill deposits and
formation of the post-ore mineral assemblage including widespread secondary uranium
minerals (Figs. 4.6E and 4.6F) occurring as fracture-filling veinlets (Fig. 4.7A).
The U 1 mineralization records an alteration event at ca. 1720 Ma, consistent with the
timing of the Oenpelli dolerite intrusion of the Kombolgie Basin (Fig. 4.16, Sweet et al.,
1999; Kyser et al., 2000). This event is coincident with the timing of post-ore alteration
event at the Ranger (1737±20 Ma, Ludwig et al., 1985, 1987) and Koongarra U deposits
(1800 Ma to 1700 Ma, Hills and Richards, 1976). Polito et al. (2004) interpreted ages of
182

1696 Ma - 1715 Ma from pre-ore sericite in altered schist at the Nabarlek deposit to be
related to resetting during intrusion of the Oenpelli dolerite at 1720 Ma.
The 1601±98 Ma model age of Gn 1 galena (Fig. 4.13A) from the Coronation Hill
deposit is coincident with formation of unconformity-related U mineralization in the
Kombolgie Basin (Fig. 4.16; e.g. Page et al., 1980; Riley et al., 1980; Maas, 1989; Polito et
al., 2004). This timing is coincident with Mesoproterozoic compressional tectonism and
metamorphism during the early Isan Orogen (1600 Ma - 1580 Ma) in northern Australia
(Hand, 2006). Peak Isan Orogen (MacCready et al., 1998) is recorded by alteration of
uraninite at ca. 1500 Ma (Fig. 4.16), which deformed the McArthur Basin (Page and Bell,
1986; Connors and Page, 1995). This event is followed by fault reactivation at ca. 1400 Ma
(Figs. 4.13B, 4.16) and is attributed to deformation related to post-peak Isan exhumation
and crustal extension (Fig. 4.16, Spikings et al., 2001). Similar U-Pb ages from Jabiluka
uraninite of 1473±40 Ma (Ludwig et al., 1985) and 1400 Ma from Nabarlek (Polito et al.
2004) are interpreted to be related to this late alteration event.
An alteration event at ca. 1300 Ma (Fig. 4.16) records widespread intrusive activity
within the Pine Creek Orogen. These events correlate with the intrusion of the
Maningkorrirr phonolitic dikes and the Derim Derim Dolerite at ca. 1316±40 and 1324±4
Ma, respectively (Sweet et al., 1999). Extensive alteration between 1200 Ma - 1250 Ma
(Fig. 4.16) corresponds to tectonic activity during the Proterozoic Australia assembly as an
early component of Rodinia, involving the amalgamation of West and North Australian
cratons, followed by collision with the South Australian craton (Myers et al., 1996). At ca.
1140 Ma (Fig. 4.16) Australia and Laurentia amalgamated during the Grenville Orogen
183

culminating with the formation of Rodinia (Wingate et al., 2002; Li et al., 2008). Alteration
of uraninite at ca. 1380 Ma and 1100 Ma is also recorded at Jabiluka and Nabarlek (Gulson
and Mizon, 1980; Polito et al., 2004).
Figure 4.16. Distribution of 207 Pb/ 206 Pb ages for 176 uraninite grains along with the timing of
various U mineralization and tectonic events that affected the South Alligator Valley area.
Alteration peaks at ca. 1000 Ma and 800 Ma (Fig. 4.16) are consistent with periods of
Rodinia breakup (Dalziel, 1991; Li et al., 2008) with the rifting of Laurentia and Gondwana
along the eastern margin of Proterozoic Australia at ca. 900 Ma-850 Ma and formation of
the Paleo-Pacific Ocean (Wingate and Giddings, 2000; Harlan et al., 2003b). These
alteration events are also recorded in uraninite from Ranger, Jabiluka, Nabarlek and
184

Koongarra, and deposits in the SAVMF (Hills and Richards, 1972; Gulson and Mizon,
1980). Subsequent fault reactivation and alteration continued into the Phanerozoic at ca.
530 Ma - 510 Ma (Fig. 4.16), coincident with the formation of Cambrian to early
Ordovician Georgina Basin (Shergold and Druce, 1980) and the extrusion of the 513 Ma
Antrim Volcanics (Hanley and Wingate, 2000) outpouring early Cambrian Plateau over
most of the North Australian Craton (Myers et al., 1996). Following a period of apparent
tectonic quiescence from the Ordovician to Devonian (Fig. 4.16), uraninite alteration
occurred during the Carboniferous coincident with tectonic activities during continental
rifting that separated Asian terranes to the north from the NW Australian Gondwana to the
south at around ca. 350 Ma - 270 Ma (Metcalfe, 2001).
Lower intercept ages in the U-Pb system of 122±90 Ma, 45±92 Ma and 23±73 Ma
(Figs. 4.12H, 4.12G and 4.12B, respectively) and recent chemical Pb ages of uraninite
(Table 4.1) record tectonic activities along the western active margin of the Australian plate
including the Mesozoic breakup between Greater India and Australia at ca. 136 Ma and
various recent collisional processes and plate boundary reorganizations north and east of
Australia during the Cenozoic (Müller et al., 2000).
4.7. Conclusions
Hydrothermal alteration, uranium mineralization, and late remobilization events have
affected rocks of the SAVMF during protracted tectonic evolution that spans over 1.8 Gyrs
(Table 4.7). Results indicate that these deposits formed at ca. 1820 Ma, subsequent to
deposition of the El Sherana Group and are therefore, older than the unconformity-related
U mineralization at 1650-1675 Ma in the Kombolgie Basin. The formation of these
185

deposits is related to fluids derived from diagenetic processes in sandstone of the El
Sherana Group and have particularly affected zones of preexisting weakness of the
basement rocks that were previously altered by a metamorphic pre-ore alteration stage. The
source of U was U-bearing minerals (monazite, apatite) in the sandstone and felsic rocks of
the El Sherana Group. The Au and PGE are derived from basement felsic and mafic rocks,
as proposed by Wyborn et al. (1997). Therefore, these deposits can be classified as
unconformity-related uranium mineralization like those in the younger overlying
Kombolgie Basin.
Results from Stewart (1965) indicate that felsic volcanic rocks of the Pul Pul Rhyolite
of the El Sherana Group have above background radioactivity. Analyses indicate
concentration of up to 25-30 ppm U in these volcanic rocks (Ayers, 1975). Fluid inclusion
data (Mernagh et al., 1994) indicate that the fluids were saline, acidic, calcium-dominated
(ca. 26 wt% CaCl 2 equiv) and highly oxidizing. Such fluids would have been particularly
favorable for uranium transport (Hedges et al., 1984) as uranyl-complexes in basinal brines
in the sandstone aquifer above the unconformity. Tectonic reactivation of the El Sherana-
Palette fault during deformation associated with the Nimbuwah event would have provided
structural conduits for hydrothermal basinal brines that descended downward into the
metamorphic basement rocks. Interaction between the oxidized U-bearing basinal brines
and the reducing carbonaceous shale of the Koolpin Formation would have led to U
reduction and precipitation. The occurrence of Au and PGE associated with quartz feldspar
porphyry at Coronation Hill may have resulted from acid neutralization and reduction
186

during fluid interaction with feldspathic host rocks (Mernagh et al., 1994), thus indicating
that ore metals deposition is also controlled by lithology composition.
Subsequent to their formation, the uranium deposits in the SAVMF have been
affected by late alteration fluid event related to both near and far-field tectonic events that
formed much of the secondary U minerals. These late events may represent incursion and
circulation of meteoric water through structurally reactivated fault zones (e.g. Kotzer and
Kyser, 1995) that remain areas of preferential fluid flow (e.g. Fayek and Kyser, 1997).
187

CHAPTER 5
GENERAL DISCUSSION
5.1. Introduction
Results presented in the preceding chapters contribute in understanding the
Proterozoic tectonic evolution and U mineralizing system in successor basins in the
Beaverlodge area of Northern Saskatchewan, Canada, and the South Alligator River area of
the Northern Territories, Australia. Based on structural, geochemical, geochronological and
petrographic relationships, this research has evaluated the character and formation of U
deposits in successor basins by detailing the relative timing relationships between
deformation and fluid events, elucidating the timing, nature and origin of ore-forming
fluids, identifying critical key structural and geochemical factors controlling U
mineralization, and presenting a conceptual genetic model for U mineralization in successor
basin areas (Fig. 5.1.).
The following elucidates the general models for uranium mineralizing systems in
Paleoproterozoic successor basins, compares them with the unconformity-related uranium
mineralization in the younger, U-rich Athabasca and Kombolgie basins and discusses the
potential implication for uranium metallogeny and exploration strategy in others
Paleoproterozoic successor basins in Finland and Guyana.
188

Figure 5.1. Generalized model for different types of U mineralizing systems manifest
in Paleoproterozoic successor basins.
5.2. Uranium mineralizing system in Paleoproterozoic successor basins: A
generalized model
Rocks underlining Paleoproterozoic successor basins in the Beaverlodge area in
Canada and the South Alligator River area in Australia record a history of dynamic
geologic events that span more than 2 Gyr. These geologic events contributed significantly
to the development of multifarious U deposits (Fig. 5.1) in these areas. Subsequent to major
deformation that affected the supracrustal rocks during the Paleoproterozoic, sedimentary
189

ed-bed strata and associated volcanic rocks were deposited in continental environments
along pre-existing faults that were reactivated during the waning stage of a major orogen.
Most of the U deposits in successor basins are structurally controlled and are affected by
repeated deformation events that affected the host rock.
In the Beaverlodge area, the Martin Lake Basin formed at ca. 1820 Ma (Langford,
1981; Morelli et al., 2001) but was immediately deformed, fractured and folded during
tectonism following the peak Trans-Hudson Orogen (Hoffman, 1990; Corrigan, 2009). The
main U mineralization event predated the deposition of the Martin Lake successor basin
and is associated with regional metamorphism and deformation during early stages of the
Trans-Hudson Orogen (Dieng et al., 2011). These deposits are classified as metamorphicrelated
uranium mineralization system (Fig. 5.1) (e.g Cuney and Kyser, 2008).
In the South Alligator River area, the El Sherana Basin formed at ca. 1830 Ma
(Jagodzinski, 1992) during crustal extension following the peak Nimbuwah event that
reactivated previous fault zones (Needham et al., 1988). The main U mineralizing event
that affected both the supracrustal rocks and sediments of the successor basin is associated
with basinal brines generated from the successor basin itself. Deposition of the El Sherana
Basin is followed by a period of relative tectonic quiescence during which time
sedimentary and associated volcanic rocks of the El Sherana group were altered by basinal
brines capable of transporting and depositing the scavenged U at the unconformity between
the basement rock and sediments of the El Sherana Basin. These deposits are variants of
unconformity-related U mineralization system (Fig. 5.1), similar to those in the younger
overlying Kombolgie Basin (e.g. Polito et al., 2004, 2006).
190

Tectonic during and immediately after basin formation plays a critical role in the
formation of unconformity-related uranium mineralization. Deformation may prevent
alteration of the successor basin sediments by inhibiting fluids circulating into the basin
thereby reducing fluid-rock interaction. This is corroborated by the weakly to unaltered
character of the Martin Lake Basin sediments that were deposited at ca. 1820 Ma during
active tectonism associated with the Trans-Hudson Orogen (Hoffman, 1989). In contrast,
deformation was less intense in the South Alligator River area during the deposition of the
El Sherana Basin at ca. 1830 Ma immediately after the peak Nimbuwah Orogen (Needham
et al., 1988), thus promoting fluid-rock interaction and alteration of the El Sherana Basin
sediments. The spatial association of U deposits with successor basins may result from the
presence of pre-existing lines of tectonic weakness that focus both near and far field
deformation and can therefore be easily reactivated, creating structural traps that are
favorable for hydrothermal fluid flow and uranium mineralization.
5.2.1. Early U mineralization
Supracrustal rocks underlying successor basins are commonly affected by multiple
tectonic events and thereby metamorphosed, granitized and intruded by granitic rocks. In
the Beaverlodge area, early U mineralization predating the formation of the successor basin
is associated with thermotectonic activities accompanied by magmatism, regional
metamorphism, and hydrothermal alteration. On the basis of their structural setting, host
rock geology, timing and style of mineralization, the early U mineralization can be divided
into two main U mineralizing systems: the granite-related U mineralization and
metamorphic-related U mineralization systems (Fig. 5.1). Similarly, based on the origin and
191

character of the fluid that formed them, early vein- and cataclasite-type mineralization can
be classified as metamorphic-related U mineralization.
5.2.1.1. Granite-related uranium mineralization
Extensional deformation during deposition of Neoarchean to Paleoproterozoic
supracrustal rocks of the Murmac Bay Group may have provided channel ways for granite
intrusions. In the Beaverlodge area, the Gunnar granite (Hartlaub et al., 2004a) was
emplaced along extensional fault systems (Fig. 5.2, Mary’s Channel and Frasier) that likely
formed during the ca. 2.35 Ga Arrowsmith Orogen (Hartlaub et al., 2007; Berman et al.,
2010), concomitant with deposition of the Murmac Bay Group (Ashton et al., 2009b). The
magmatic-related U mineralization in the Gunnar deposit produced about 7,420 t of U
metal from ores grading 0.15% U (Evoy, 1986). Isotopic compositions of syn-ore minerals
indicate that the U mineralization was derived from magmatic fluids that exsolved from the
albitized granitic rock itself during its emplacement (Fig. 5.1). Uraninite formed when
reduced and cooling exsolved residual hydrothermal magmatic fluids near 315 o C were
deposited in voids left after quartz and calcite dissolution. The loss of a large volume of
CO 2 during magmatic-fluid degassing controlled U precipitation. However, the U
associated with the granite-related mineralization is minor in the deposit and is overprinted
later by more substantial breccia-type U mineralization. The metasomatism that affected the
granite produced an albitized rock that is more competent than the surrounding rocks and
therefore capable of focusing brittle reactivation caused by tectonic events. The age of the
magmatic-related U mineralization at Gunnar is not known with certainty because of the
multiple late fluid events that affected the uraninite, but it can be bracketed between the age
192

of the 2321±3 Ma Gunnar granite and the age of the 1.85 Ga major brecciation event that
overprinted the mineralized albitized granite.
Figure 5.2. Geologic cross-section through the Gunnar deposit (modified from Evoy, 1960)
The metasomatic-type U mineralization at Gunnar is genetically linked to the albite
metasomatism of the Gunnar granite because all of it was derived from the same magmatichydrothermal
alteration process. Ashton (2010) reported albite metasomatic alteration
associated with U mineralization at several localities in the Beaverlodge area but suggested
that this alteration affected a variety of rock types of different ages. There are a number of
granite intrusions in the Beaverlodge area that are coeval with the Gunnar granite, including
the Cameroon, Mackintosh Bay, Rogers Lake and White granites (Fig. 2.2). Whether the
same hydrothermal magmatic-related U mineralization system affected these granites is
currently not known.
193

5.2.1.2. Metamorphic-related uranium mineralization
5.2.1.2.1. Early-vein and cataclasite-type uranium mineralization
Minor U mineralization associated with early veins and cataclasite in the Beaverlodge
area formed at ca. 2.29 Ga during late stages of the ca. 2.35 Ga Arrowsmith Orogen and
was triggered by reactivation of basement-rooted shear zones during exhumation, resulting
in overprinting of mylonite by cataclasite and early tensional veins (Fig. 5.3; Dieng et al.,
2011). The δ 13 C and δ 18 O values and chlorite crystal chemistry of syn-ore minerals are
consistent with formation of Ca-F-Mg-rich fluids at ca. 310 o C derived from retrograde
metamorphic processes during exhumation and erosion of the supracrustal rocks. Hydraulic
fracturing and hydration during decompression and exhumation is interpreted as the main
mechanism for the early tensional vein formation. The associated pressure decrease and
fluid decompression during fracturing changed the stability of the U-carbonate complexes,
decreased the temperature of the fluids, and likely promoted U precipitation into fractures.
Although this style of U mineralization is limited, it indicates that the Beaverlodge area
probably had elevated reserves of leachable U.
5.2.1.2.2. Breccia-type uranium mineralization
The major event of U mineralization in the Beaverlodge area coincided with massive
brecciation at ca. 1850 Ma triggered by reactivation of fault zones that breached the host
rock (Fig, 5.3) during the early stages of the Trans-Hudson Orogen. The δ 18 O, δ 13 C and δ 2 H
values and chlorite crystal chemistry of syn-ore minerals indicate that the ore-forming
brines originated from a ca. 330 o C, Ca-Na-F-containing metamorphic-hydrothermal fluid.
194

Figure 5.3. Schematic illustration of the tectonic evolution of the Main Ore Shear Zone and
the Saint Louis Fault on a crustal scale showing the spatial distribution of breccias, cataclasite
and mylonite. A: Mylonitisation with oblique-normal and lateral dextral sense of motion in
the ductile environment. B: Cataclasite overprinted the ductile shear zones subsequent to
exhumation of the fault zone to shallower crustal depths. C: Breccias formed during
reactivation the ductile-brittle fault zone in the brittle environment presumably at near
surface conditions.
These fluids were likely derived from dehydration of hydrous minerals and ascended
upward along fracture systems and dilatant jogs that resulted from brittle reactivation of
early shear zones (Fig. 5.3), thus providing pathways for metamorphic fluids that
scavenged and transported U-bearing fluids (Fig. 5.1). Uranium precipitation in the breccia
system was likely caused by a decrease in the solubility of the U-carbonate complexes
resulting from a loss of CO 2 and a decrease in temperature caused by fluid decompression
195

during brecciation or reduction as the U-mineralizing fluid reacted with reducing
metamorphic host rocks (e.g. Skirrow et al., 2009).
Strong structural control is reported in most metamorphic-related U systems, with U
originating from saline, F-rich and CO 2 -bearing, Na-Ca brines (Skirrow et al., 2009) and
commonly hosted by reactivated fault zones (Cuney and Kyser, 2008). In the Beaverlodge
area, the high δ 18 O values of metamorphic fluids reflect the low water/rock ratios, and
hence the relatively low volume of fluid, during hydrothermal alteration, preventing the
transport of enough U by metamorphic brines to produce economically significant U
mineralization. This is consistent with Plant et al. (1999) suggestion that U deposits of
metamorphic-dehydration origin are of low grade and tonnage. The Beaverlodge U deposits
are similar to metamorphic-related U mineralization systems associated with Nametasomatism
(Cuney and Kyser, 2008) and related to the global 1.9-1.75 Ga alkalimetasomatism
(Cuney, 2010).
5.2.2. Successor basin-related U mineralization
5.2.2.1. Volcanic-related U mineralization
Volcanic-related U mineralization in the Beaverlodge area was triggered by extrusion
of the 1818±4 Ma alkaline mafic dikes (Morelli et al., 2009) during deposition of the
Martin Lake Basin (Langford, 1981; Mazimhaka and Hendry, 1984). Extrusion of the mafic
dikes is coincident with periods of active tectonism related to back-arc extension following
peak Trans-Hudson Orogen (Hoffman, 1989; Corrigan, 2009). The δ 18 O, δ 13 C and δ 2 H
values and chlorite crystal chemistry of syn-ore minerals indicate that the U mineralization
formed at ca. 1820 Ma from ca. 320°C, Mg- and Fe-rich magmatic fluids that were likely
196

exsolved from the mafic dikes during their emplacement (Fig. 5.1). Faulting and fracturing
of the host rock during extrusion of the mafic dikes provided pathways for exsolved
magmatic-hydrothermal mineralizing solutions. The key geochemical process leading to U
deposition was changes in the pH or Eh state of the mineralizing solution through
interaction between the magmatic hydrothermal brine and fluids resident in metamorphic
host rocks that destabilized the uranyl-phosphate complexes.
5.2.2.2. Unconformity-related U mineralization
Minor U-veins associated with fluids generated in the 1750 Ma Athabasca Basin
(Kyser et al., 2000) formed at ca. 1620 Ma in the Beaverlodge area and were triggered by
tectonic reactivation of fault zones during the Mesoproterozoic Mazatzal Orogen (Eisele
and Isachsen, 2001). This deformation caused minor faulting and fracturing of the basement
and basin rocks followed by deposition of Athabasca-type U-mineralization observed in the
Ace-Fay and Martin Lake deposits (Dieng et al., 2011). δ 18 O and δ 2 H values and chlorites
crystal chemistry of syn-ore chlorite indicates that U mineralization formed oxidizing
basinal brines near 235°C, identical to those of the unconformity-related U-deposits in the
Athabasca Basin (e.g. Fayek and Kyser, 1997). Syn-ore mineral crystal chemistry indicates
that F - , Chl - , CO 2- 3 , and PO 3- 4 were likely present in the ore assemblage and could be
effective ligands for complexing U. The key process controlling U deposition in vein
systems was likely reduction of the oxidizing U-bearing basinal brines through interaction
with reducing basement lithologies (e.g. Hoeve and Quirt, 1984; Cuney and Kyser, 2008).
U mineralization in the El Sherana Basin in the South Alligator River area coincided
with a hydrothermal alteration event during later stages of the Nimbuwah tectonic event at
197

ca. 1820 Ma that triggered reactivation of the El Sherana-Palette fault system (Lally and
Bajwah, 2006). Faulting and brecciation was likely more focused in zones of pre-existing
tectonic weakness that were previously affected by pre-ore alteration, thus creating
structural traps near the unconformity that were open to fluid flow, hydrothermal alteration
and U mineralization. The mineralization formed when a 250 o C, low latitude, oxidizing, U-
bearing basinal brine from diagenetic aquifers in the Coronation sandstone, similar to those
of unconformity-related U-deposits in the Athabasca (e.g. Cuney and Kyser, 2008) and
Kombolgie basins (e.g. Polito et al., 2004, 2006), descended downward into the
unconformity along fracture systems created by brittle reactivation of the El Sherana-
Palette fault system (Fig. 5.1). At Coronation Hill, the mineralizing brine contained U, Au
and PGE, the former most likely leached from detrital U-bearing minerals in the El Sherana
Basin sandstone, and the Au and PGE from alteration of felsic volcanics and mafic rocks
that are part of the El Sherana Group (Jagodzinski, 1992). Interaction of oxidizing basinal
brines with the reducing Fe-rich ferruginous shale of the Koolpin Formation may have led
to deposition of the U-ore metals at El Sherana. The U, Au and PGE ore associated with the
quartz feldspar porphyry at Coronation Hill may have resulted from acid neutralization and
moderate reduction caused by fluid interaction with feldspathic host rocks (Needham,
1988b; Wyborn, 1992; Mernagh et al., 1994).
5.2.3. Late alteration events
Subsequent to their formation, U deposits in the Beaverlodge and South Alligator
River areas were affected by alteration events associated with multiple stages of
deformation and fluid events that are related to both near and far-field geodynamic events
198

and coincident with the timing of major thermotectonic events that have affected these
areas. Results show that periods of alteration and remobilization events recorded over 2 Gyr
of tectonic evolution of the North American Shield and the Australian craton.
Early vein and cataclasite-type U mineralization in the Beaverlodge area was
significantly affected by the 2.2-2.1 Ga and 2.1-2.0 Ga tectonism coincident with a period
of rifting related to the breakup of the Kenorland supercontinent (Williams et al., 1991).
This event is followed by the 2.0-1.9 Ga period of alteration during the Taltson-Thelon
Orogen (Chacko et al., 2000) and activation of the Snowbird Tectonic Zone (Berman et al.,
2007a).
A major event, which has significantly reactivated structures in the Beaverlodge area,
corresponds to the Trans-Hudson Orogen, which produced brecciation along reactivated
fault zones, fluid flow and the major U mineralization. This mineralization has been altered
during intracratonic deformation following the peak Trans-Hudson Orogen and formation
of the Martin Lake Basin (Mazimhaka and Hendry, 1985). The event has produced the
volcanic-type mineralization and subsequent alteration during emplacement of 1788±3 Ma
lamprophyre (Sassano et al., 1974) and granitic dikes (Ashton et al., 2009b).
Late brittle reactivation along fault zones during the Mesoproterozoic caused minor
fracturing and alteration of preexisting mineralization and records tectonism of the 1.65-
1.60 Ga Mazatzal Orogen in southern Laurentia (Labrenze and Karlstrom, 1991).
From the Mesoproterozoic to recent time, far field tectonic events of several
orogenic episodes during the evolution of the Laurentian plate (e.g. Evans and Pisarevsky,
2008) caused minor brittle reactivation in the Beaverlodge area. These include the Granite
199

Plutons Event at 1.4 Ga (Barinek et al., 1999), the 1.27 Ga Mackenzie mafic dike swarms
(Ernst and Buchan, 2001b) coincident with the final breakup of the Nuna supercontinent
(Rogers and Santos, 2002), the Grenville Orogen at ca. 1.2–0.9 Ga (Carr et al., 2004)
reflecting the assembly of Rodinia (Moores, 1991), the diachronous breakup of Rodinia at
0.7-0.8 Ga and 0.6-0.5 Ga (Li et al., 2008), and the Appalachian Orogen at 0.3-0.4 Ga
linked to Pangea assembly (Cocks and Torsvik, 2002). Lower intercept ages in the U-Pb
system reflect tectonic activity during the Cordilleran Orogen (Molnar and Atwater, 1978)
and recent reactivation during the Pleistocene glaciations (Adams, 1989).
In the South Alligator River area, deposits also have been significantly affected by
late fluid events related to fault reactivation during successive regional thermotectonic
events that occurred over a period of at least 1.8 Gyrs. The first coincided with the timing
of the ca. 1720 Ma Oenpelli dolerite intrusion (Sweet et al., 1999). Uraninite from the
Coronation Hill deposit record the Isan Orogen (1600-1580 Ma) in northern Australia
(Hand, 2006), shortly after formation of unconformity-related U mineralization in the
Kombolgie Basin (Polito et al., 2004). From the Mesoproterozoic to recent time, far field
tectonic events affected deposits in the South Alligator River area as discussed in a greater
detail in Chapter 4.
Electron microprobe analyses of various chlorite phases in deposits of the
Beaverlodge and South Alligator River areas indicate also that these deposits were
subsequently altered to low-temperature, recording the effect of late fluid events. These
events may represent incursion and circulation of meteoric water through fault zones
(Kotzer and Kyser, 1995). Hydrogen isotopic composition of chlorites in the Beaverlodge
200

area record retrograde exchange of H-isotopes with relatively recent meteoric water having
low δ 2 H values (e.g. Kyser and Kerrich, 1991). The preferential exchange of H-isotopes in
these chlorites suggests that the fault zones were active after U-mineralization and remain
a zone of preferential fluid circulation (e.g. Fayek and Kyser, 1997).
5.3. Implication for uranium metallogeny in others Paleoproterozoic successor
basins: the case of Finland and Guyana
U mineralization in Paleoproterozoic successor basins similar to those in the
Beaverlodge and South Alligator River areas are also known in Finland and Guyana.
5.3.1. Uranium metallogenic in Paleoproterozoic successor basins in Finland
Rocks of the Fennoscandinavian shield in central Finland (Fig. 5.4) are divided into
the Karelian and Kola domains separated by the Lapland granulite belt (Sorjonen-Ward et
al., 1994). The Kola domains comprise Archean and Paleoproterozoic terrains that were
accreted to the Karelian domain between 2 Ga and 1.8 Ga (Sorjonen-Ward and Luukkonen,
2005) and consist of granitoids and gneisses (Gaál and Gorbatschev, 1987). The 2.5-1.85
Ga Karelian domain consists of Neoarchean basement and Paleoproterozoic sedimentary
rocks with minor volcanic rocks and occurs in separate basins within Neoarchean basement
blocks.
201

Kolari-Kittila
Province
Kuusamo
Province
Muhos
Basin
Koli
Province
Satakunta
Basin
Uussimaa
Province
Figure 5.4. Bedrock of Finland showing the location of Mesoproterozoic basins and successor
basin U provinces. Map from Geological Survey of Finland.
The early Paleoproterozoic Karelian rocks in the Koli province (Fig. 5.4) have been
affected by amphibolite facies metamorphism and cut by 2.1–1.97 Ga tholeitic and 2.2 Ga
spilitic intrusions (Saltikoff et al., 2006) (Fig. 5.5). The Karelian stratigraphy comprises the
Sariolan (2.5–2.3 Ga), Jatulian (2.3–2.0 Ga), and Kalevan (2.0–1.9 Ga) units (Fig. 5.5; äikä,
202

2006) that likely formed during rifting and breakup between 2.5 Ga and 2.0 Ga that
strongly affected and partly dispersed the Archean domains (Gorbatschev and Bogdanova,
1993). Sedimentary rocks of the Jatulian lower sequence (Fig. 5.5) constitute a successor
basin to this major tectonic event and are later inverted during the 1.95-1.82 Ga
Svecofennian Orogen (Pharaoh and Brewer, 1990), exhumed and overlain by the late
Mesoproterozoic Satakunta Basin at ca.1.4–1.3 Ga (Simonen, 1980).
Figure 5.5. Schematic Karelian stratigraphy, lithology, and uranium occurrences in the Koli
area, eastern Finland, showing location of various U deposits (modified from Piiarinen (1968),
Merlainen (1980) and Äikä (2006))
In the Koli domain, six U deposits are known within the lower quartzite and middle
arkosite member of the Jatulian unit (Fig 5.5, Äikä, 2006).
203

The uranium deposits in various provinces shown in Fig. 5.4 have been interpreted as
epigenetic in origin with fluid probably originated from the Archean granitoids and
associated Paleoproterozoic rocks (Äikä and Sarikkola, 1987). The U mineralization occurs
as: (1) lenses and disseminations in the quartz-pebble conglomerate in quartzite and
arkosite members, (2) near the contact between the Jatulian diabase dikes and the basal
conglomerate where they cut the uraniferous quartzite-conglomerate horizon, and (3) at the
unconformity between the Sariolian basement rocks and the basal conglomerate of the
lower Jatulian unit (Fig.5.5).
Recent geochronological studies suggest that the age of the Jatulian U mineralization
is close to ca. 2273 Ma (K. Kyser, pers. Comm.2012) with extensive late alteration related
to subsequent tectonic events such as the dominant 1.95-1.82 Ga Svecofennian Orogen
(Pharaoh and Brewer, 1990). The age of the U mineralization in this successor basin is
therefore older than the overlying late Mesoproterozoic Satakunta sandstones deposited at
1.4-1.3 Ma (Fig. 5.4). Aikas and Sarikkola (1987) suggested that mineralogical and
geochemical evidence indicate multistage epigenetic U mineralization in these deposits.
Äikä and Sarikkola (1987) and Saltikoff et al (2006) suggested some similarities with
known economically important, unconformity, vein, breccia, and sandstone deposit styles.
The styles of U mineralization spatially associated with Jatulian successor basins in
the Koli area, the occurrence of U at the basal Jatulian unconformity, the close association
between the U mineralization and the 2.1–1.97 Ma mafic dikes, and U occurrences as
disseminations in metamorphosed conglomerate of the Jatulian quartzite and arkosite
members (Fig. 5.5), suggest many similarities between these deposits and U deposits
204

associated with the Martin Lake successor Basin in the Beaverlodge area and El Sherana
Basin in South Alligator River area. U mineralization at the basal Jatulian unconformity
may have formed from fluid originating from diagenetic processes in the overlying basal
quartzite and conglomerates of the lower Jatulian sequence similar to deposits in the South
Alligator River area. U mineralization in close association with the mafic dikes are similar
to those of volcanic-type associated with the Martin Lake mafic dikes in the Beaverlodge
area. Uranium mineralization disseminated in the metamorphosed conglomerate of the
quartzite and arkosite members could have originated from remobilization of pre-existing
uranium enrichments from the Sariolian rocks along fault zones (K. Kyser, pers. Comm.
2012).
The occurrence of early U mineralization associated with the Jatulian successor basin
could be a favorable indication for the presence of unconformity-related U mineralization
in the younger overlying late Mesoproterozoic basins in the Karelia region of Finland, as
the early U mineralization in the successor basin could be a potential source for detrital
uraninite in younger Mesoproterozoic basins, such as the Satakunta Basin (Fig. 5.4).
5.3.2. Uranium metallogeny in Paleoproterozoic basins in Guyana
The Roraima Basin was deposited in a large Paleoproterozoic foreland basin in
northern South America. The basin covers a large area in Brazil, Venezuela, Guyana,
Suriname, and Colombia (Fig. 5.6) and consists mostly of horizontal and gently dipping
fluvial sandstones (Santos al., 2003).
205

Fig. 5.6. Distribution of the Roraima Supergroup and outliers in northern South America
(modified from Santos et al., 2000).
This broad region comprises five geologic provinces of different age and structural
settings: the Archean Imataca province and the Proterozoic Trans-Amazon, Tapajo´s-
Parima, Central Amazon, Rio Negro, and Sunsa´s provinces (Santos et al., 2000). Roraima
Basin sedimentary rocks consist principally of sandstone derived from the 2.25–2.0 Ga
Trans-Amazonian granitoid-greenstone basement rocks (Santos et al., 2000; Gibbs and
Olszewski, 1982), to the north and northeast and deposited in braided, deltaic, and shallow
marine environments (Reis et al., 1990). These sediments overlap sandstones of the post-
Roraima Neblina successor foreland basin (Pinheiro et al., 1976), which was also derived
206

from both the Trans-Amazon and Tapajo´s-Parima orogenic belts to the east and northeast
(Santos al., 2003). The minimum age of the Roraima Basin was determined by U-Pb
geochronology from mafic sills to be 1782±3 Ma (Santos et al., 2003).
A number of U showings are spatially associated with the Roraima Basin. These
include the Aricheng albitite-hosted U mineralization (Fig. 5.7) and several other
occurrences hosted by the Kurupung Batholith in the basement near the Roraima Basin, in
western Guyana (Cinelu and Cuney 2006; Alexandre, 2010).
The Aricheng deposit is geologically similar to albitite-hosted deposits worldwide
(Cinelu and Cuney 2006, Alexandre, 2010). The Lagoa Real and Espinharas U deposits in
Brazil have host rocks that resemble those of around Kurupung Batholith in the Aricheng
deposit. Syn-ore hydrothermal zircon gives a minimum age of 1995±15 Ma for the U
mineralization (Alexandre, 2010), which is older than the age of the Roraima Basin. The
timing and style of U mineralization in the Aricheng deposit (Cinelu and Cuney 2006,
Alexandre, 2010) in Guyana and Lagoa Real (Lobato and Fyfe, 1990) and Espinharas
deposits (Porto de Silveira et al. 1991) in Brazil are similar to those of the granite-related U
mineralization in the Beaverlodge area (Dieng et al., 2011). This early U mineralization
associated with the underlying basement rock in the Roraima Basin could have been a
potential source for detrital uraninite in the younger Paleoproterozoic Roraima Basin as
most of the detritus in the basin were derived from Trans-Amazonian granitoids (Orestes
al., 2003) that host most of the U deposits in the successor basins.
The presence of early U mineralization in successor basins is thus a favorable
indication for unconformity-related U mineralization in the younger Paleoproterozoic
207

Roraima Basin, similar to what is observed in the Beaverlodge area in Canada, the South
Alligator River area in Australia, and the Koli province in eastern Finland
Fig. 5.7. Geological map of the Aricheng occurrence with the major geotectonic units in South
America (top) and with the major rock types observed in its vicinity in western Guyana
(bottom) (modified from Alexander et al., 2010).
208

CHAPTER 6
CONCLUSIONS
An integrated multidisciplinary geological study, including structural geology,
geochronology, petrographic and geochemistry approaches, was used to detail the structural
and fluid evolution of uranium deposits in successor basins in the Beaverlodge area in
Canada, and the South Alligator River area in Australia.
The results presented in this research demonstrate that:
a) The Beaverlodge area in Canada and the South Alligator River area in Australia record
ore-forming systems that resulted from multistage deformation, hydrothermal
alteration, U mineralization, and late fluid processes during protracted tectonic
evolution that spans over 2.3 Gyr.
b) The main breccia-type U mineralizing event that affected all deposits in the
Beaverlodge area formed at ca. 1850 Ma from Ca-Na-dominated metamorphic fluids at
ca. 330 o C linked to metasomatism accompanying regional metamorphism of the Trans-
Hudson Orogen. The ore-forming fluids were likely derived from metamorphic
remobilization of pre-existing U-rich basement rocks, and ascended upward along deep
fracture systems that resulted from brittle reactivation of early ductile shear zones. U
precipitated when decompression during brecciation decrease the solubility of the U-
carbonates complexes and the temperature of the fluid.
c) Early minor stages of U mineralization in the Beaverlodge area are hosted in
cataclasite and veins at ca. 2.29 Ga and in albitized granite in the Gunnar deposit
209

etween ca. 2.3 Ga and 1.9 Ga. Later stages are related to minor U veins at ca. 1.82 Ga
linked to Martin Lake mafic dikes and to minor late veins at ca. 1.62 Ga corresponding
to the timing of unconformity-type U mineralization in the Athabasca Basin.
d) The main event of U mineralization in the South Alligator River area formed at ca.
1820 Ma, subsequent to deposition of the El Sherana Group at 1840-1830 Ma. The
formation of these deposits is related to fluids derived from diagenetic processes in
sandstone of the El Sherana Group. The source of the ore was likely U-bearing
minerals in the sandstone and volcanic rocks of the El Sherana Group and the source of
metals such as Au and PGE are from basement rocks, similar to some of the multielement
deposits (i.e. Nicholson) in the Beaverlodge area of Canada. These deposits
can be classified as a variation on unconformity-related U mineralization similar to
those in the overlying Kombolgie Basin. Tectonic reactivation of the El Sherana-
Palette fault during the Nimbuwah event would have provided structural conduits for
hydrothermal basinal brines that descended downward into the metamorphic basement
rocks. Interaction between the oxidizing U-bearing basinal brines and the reducing
carbonaceous shale of the Koolpin Formation would have led to U precipitation.
Uranium deposits in the Beaverlodge and South Alligator River areas record late
alteration fluid events related to both near and far-field tectonic events. These late
events represent circulation of meteoric water through fault zones.
e) Uraninite in major structures is greatly sensitive to fluid events stimulated by both
near- and far-field tectonic events. It can serve as vehicle to understand the complex
210

timing relationships between fault activities, hydrothermal and ore-forming processes
to regional thermotectonic events.
f) Uranium deposits in the Beaverlodge and South Alligator River area are older than
those in the U-rich Athabasca and Kombolgie basins. Rocks that host these deposits
have been folded and exhumed during subsequent tectonic events. These older U
deposits can be considered as a potential source for detrital uraninite that fed sediments
of the Athabasca and Kombolgie basins and therefore contributed to the inventory of
uranium that formed unconformity-related U mineralization in the younger basins.
g) Uranium deposits in the Beaverlodge and South Alligator River areas share many
similarities with those associated with the Jatulian successor basin of the
Fennoscandinavian shield of central Finland. The overlying late Mesoproterozoic
Satakunta Basin can be considered as being a potential basin to host unconformityrelated
U mineralization similar to those in the Athabasca and the Kombolgie basins.
Similarly, the Roraima basin in Guyana has also potential to host unconformity-related
U mineralization.
h) The occurrence of older U mineralization associated with successor basins and
basement lithology can be considered as a new criterion for exploration of
unconformity-related uranium mineralization in younger Paleoproterozoic basins.
211

REFERENCES
Adams, J., 1989. Postglacial faulting in eastern Canada: Nature, origin and seismic hazard
implications. Tectonophysics 163, issue 3-4, 323-331.
Ahmad M, Lally J.H., McCready A.J., 2006. Economic geology of the Rum Jungle Mineral
Field, Northern Territory. Northern Territory Geological Survey, Report 19.
Äikä, O and Sarikkola, R., 1987. Uranium in lower Proterozoic conglomerates of the Koli
area, eastern Finland. In: Uranium deposits in Proterozoic quartz-pebble
conglomerates. IAEA-TECDOC-427, Wien, pp. 189–234.Aldrich, L. T. and
Wetherill, G. W., 1956. Evaluation of mineral age measurements, I and II.
National Research Council Science 19, 147-156.
Äikä, O., 2006. Uranium in Finland: Geology, deposits & exploration. http://www.atsfns.fi/archive/esitys_aikas.pdf
Alexandre P. and Kyser K., 2005. Effects of cationic substitutions and alteration of
uraninite and implications for the dating of uranium deposits. Canadian
Mineralogy 43, 1005–1017.
Alexandre P., Kyser K., Thomas D., Polito P., Marlat J., 2007. Geochronology of
unconformity-related uranium deposits in the Athabasca Basin, Saskatchewan,
Canada and their integration in the evolution of the basin. Mineralium Deposita.
44-1, 41-59.
Alexandre P., Kyser K., Thomas D., Polito P., Marlat J., 2009, Geochronology of
unconformity-related U deposits in the Athabasca Basin, Saskatchewan, Canada
and their integration in the evolution of the basin: Mineralium Deposita, v. 44-1,
p. 41-59.
Alexandre, P., 2010. Mineralogy and Geochemistry of Sodium Metasomatism-Related
Uranium Occurrence of Aricheng South, Guyana,” Mineralium Deposita, Vol.
45, No. 4, pp. 351-367.
Alexandre P., Kyser K., Layton-Matthews D., 2010. REE concentrations in zircon and the
origin of U in the unconformity-related U deposits in the Athabasca Basin,
Canada: GeoCanada 2010, 10-14 May, Calgary, Canada.
Allen, J. A., 1963. Structural control of the 01 and 09 orebodies, Ace and Fay mine,
Beaverlodge, Saskatchewan. Unpublished M.Sc. Queen’s University, Kingston,
Ontario, Canada, 70p.
Ansdell, K.M. and Yang, H., 1995. Detrital zircons in the McLennan Group meta-arkoses
and MacLean Lake belt, western Trans-Hudson Orogen: In Hajnal, Z., Lewry, J.
212

(Eds.). Lithoprobe Trans-Hudson Orogen Transect Report 48, Lithoprobe
Secretariat, University of British Columbia, pp. 190–197.
Ansdell, K.M., Corrigan, D., Stern, R., Maxeiner, R., 1999. Shrimp U–Pb geochronology
of complex zircons from Reindeer Lake Saskatchewan: implications for timing
of sedimentation and metamorphism in the northwestern Trans-Hudson Orogen.
Geological Association of Canada. Abstract 24, 3–4.
Ansdell, K.M., 2005. Tectonic evolution of the Manitoba-Saskatchewan segment of the
Paleoproterozoic Trans-Hudson Orogen, Canada. Canadian Journal of Earth
Sciences 42, 741-759.
Ashton, K. E. and Card, C. D., 1998. Rae northeast: a reconnaissance of the Rae province
northeast of Lake Athabasca. Saskatchewan Geological Survey. Miscellaneous
Report 98-4, 3–16.
Ashton, K. E., Kraus, J., Hartlaub, R. P., Morelli, R., 2000. Uranium City revisited: a new
look at the rocks of the Beaverlodge Mining Camp. Saskatchewan Geological
Survey. Miscellaneous Report 2000-4, 2 3–15.
Ashton, K. E., Boivin, D., Heggie, G., 2001. Geology of the southern Black Bay Belt, west
of Uranium City, Rae province. Saskatchewan Geological Survey, Miscellaneous
Report 2001-4, 50–63.
Ashton, K.E., Hartlaub, R.P., Heaman, L.M., Morelli, R., Bethune, K.M., Hunter, R.C.,
2004. Paleoproterozoic sedimentary successions of the southern Rae Province:
Ages, origins and correlations: Geological Association Canada/Mineralogy
Association Canada, Jt. Annual Meeting., St. Catharines, Abstract. V., CD-ROM,
p. 434.
Ashton, K.E. and Hartlaub, R.P., 2008. Geological compilation of the Uranium City area.
Saskatchewan Ministry of Energy and Resources, Open File 2008-5, set of four
1:50 000- scale maps.
Ashton, K.E., Hartlaub, R.P., Heaman, L.M., Morelli, R.M., Card, C.D., Bethune, K.,
Hunter. R.C., 2009a. Post-Taltson sedimentary and intrusive history of the
southern Rae province along the northern margin of the Athabasca Basin,
Western Canadian shield. Precambrian Research 175, 16-34.
Ashton, K.E., Rayner, N.M., Bethune, K.M., 2009b. Meso- and Neoarchean Granitic
Magmatism, Paleoproterozoic (2.37 Ga and 1.93 Ga) Metamorphism and 2.17
Ga Provenance Ages in a Murmac Bay Group Pelite; U-Pb SHRIMP Ages from
the Uranium City Area. In Summary of Investigations, 2009. v. 2, Saskatchewan
Geological Survey, Saskatchewan Ministry of Energy and Resources,
Miscellaneous Report, 2009-4,2, Paper A-5, 9p.
213

Ashton, K.E., 2010. The Gunnar Mine: an episyenite-hosted, granite-related uranium
deposit in the Beaverlodge uranium district; in Summary of Investigations 2010
Volume 2,. Saskatchewan Geological Survey, Saskatchewan Ministry of Energy
and Resources, Miscellaneous Report, 2010-4,2, Paper A-4, 21p.
Ayres, D.E. and Eadington P.J., 1975. Uranium Mineralization in the South Alligator
ValleyValley. CSIRO Division of Mineralogy, Sydney, Aust. Min. Deposita
Berl.. 10, 27-41.
Baldwin, J.A., Bowring, S.A., Williams, M.L., 2003. Petrological and geochronological
constraints of high pressure, high temperature metamorphism in the Snowbird
tectonic zone, Canada. Journal of Metamorphic Geology 21, 81–98.
Barinek, M. F., Foster C. T., Chaplinsky P. P., 1999. Metamorphism and deformation near
the N 1.4-Ga Mount Ethel pluton, Park Range, Colorado. Rocky Mountain
Geology 34, 21-35.
Beck, L.S., 1969. Uranium Deposits of the Athabasca Region, Saskatchewan.
Saskatchewan Department Mineral Resources 126, 139p.
Beecham, A.W., 1969. A structural study of the ABC fault, Beaverlodge, Saskatchewan.
Unpublished M.Sc. thesis, Queen’s University, Kingston, Ontario, Canada 80p.
Belevtsev, Y.N. and Koval, V.B., 1968. Genesis of U deposits associated with sodium
metasomatism in crystalline rocks of shields: Geologicheskiy Zhurnal (Kiev.) v.
28, p. 4-17.
Bell, K., 1981. A review of the geochronology of the Precambrian of Saskatchewan- some
clues to uranium mineralization Mineralogical Magazine. Vol. 44, 371-378.
Bergeron, J., 2001. Deformation of the Black Bay structure: Unpublished M.Sc. Thesis,
University of Saskatchewan, Saskatoon, Saskatchewan.
Bergeron, J., Stauffer, M., Ansdell, K., 2002. The Black Bay deformation zone, Rae
province, Canadian Shield: Archean ductile deformation to Paleoproterozoic
brittle slip; 900 my of reactivation. Geological Association Canada – Mineralogy
Association Canada, Program with Abstract, 27, 8.
Berman, R.G., Sanborn-Barrie, M., Stern, R.A., Carson, C., 2005. Tectono-metamorphism
at ca. 2.35 and 1.85 Ga in the Rae domain, western Churchill province, Nunavut,
Canada: insights from structural, metamorphic and in situ geochronological
analysis of the southwestern Committee Bay belt. Canadian Mineralogy 43, 409–
442.
214

Berman, R.G., Davis, W.J., Pehrsson, S., 2007a. The collisional Snowbird tectonic zone
resurrected: growth of Laurentia during the 1.9 Ga accretionary phase of the
Trans-Hudson Orogen. Geology 35, 911–914.
Berman, R.G., Ryan, J.J., Davis, W.J., Nadeau, L., 2008. Preliminary results of linked insitu
SHRIMP dating and thermobarometry studies in the Boothia mainland area,
north-central Rae province, Nunavut. Geological Survey of Canada 2, 1–13.
Berman, R.G., Sandeman, H.A.I., Camacho, A., 2010. Diachronous deformation and
metamorphism in the Committee Bay belt, Rae province, Nunavut: insights from
40Ar–39Ar cooling ages and thermal modeling: Precambrian Research181,
Issues 1-4, 1-20.
Bethune, K.M., 1997. The Sudbury dike swarm and its bearing on the tectonic development
of the Grenville Front, Ontario, Canada: Precambrian Research 85, 117-146.
Bethune, K.M., Ashton, K.E., Berman, R.G., Knox, B., 2008. U–Pb SHRIMP
geochronology in the western Beaverlodge Domain, Saskatchewan: unraveling
the polyphase tectono-metamorphic history of the SW Rae province. GAC–MAC
2008 Abstract, 33, 21.
Bethune, K., Ashton, K. E. and Knox, B., 2010. Tectonic evolution of the Beaverlodge
domain, SW Rae province, based on structural, petrological and
geochronological study: implications for the nature and extent of Taltson (-
Thelon) Orogen and the origin of the Snowbird tectonic zone. Geocanada, 2010,
Calgary, Canada.
Beyer, S. R., 2011, Basin analysis and the evaluation of critical factors for unconformityrelated
U mineralization, Paleoproterozoic western Thelon and Otish basins,
Canada: Unpublished Ph.D. thesis, Queen’s University Kingston, Ontario,
Canada, 230 p.
Bilal, B.A. and Koss, V., 1980a, Studies on the distribution of fluoro complexes of rare
earth elements in fluorite bearing model systems: Journal of Inorganic and
Nuclear Chemistry, v. 42, p. 629-630.
Bogdanova, S. V., Pisarevsky, S. A., Li, Z. X., 2009. Assembly and Breakup of Rodinia
(Some Results of IGCP Project 440): Stratigraphy and Geological Correlation
17, 259–274.
Bostock, H.H. and van Breemen, O., 1992. The timing of emplacement and distribution of
the Sparrow diabase dike swarm, District of Mackenzie, Northwest Territories:
In Radiogenic Age and Isotopic Studies: Report 6, Geological Survey of Canada
92-2, 49-55.
215

Bowles, J.F.W., 1990. Age dating of individual grains of uraninite in rocks from electron
microprobe analyses. Chem. Geology. 83, 47-53.
Capuano R.M., 1992. The temperature dependence of hydrogen isotope fractionation
between clay minerals and water: Evidence from a geopressured system.
Geochim. Cosmochim. Acta 56, 2547–2554.
Card, C.D., Pana, D., Portella, P., Thomas, D.J., Annesley, I.R., 2007. Basement rocks to
the Athabasca Basin, Saskatchewan and Alberta, in: EXTECH IV, Geology and
Uranium Exploration Technology of the Proterozoic Athabasca Basin,
Saskatchewan and Alberta. Geological Survey Canada, Bulletin. 588, pp. 193–
209.
Carr, S.D., Easton, R.M., Jamieson, R.A., Culshaw, N.G. and White, D.J., 2004. The
Grenville Orogen of Ontario and New York—a Himalayan-scale mountain belt:
Significance of along strike-variations: In: The Celebratory Conference, From
Parameters to Processes—Revealing the Evolution of a Continent, October 12-
15, 2004, Toronto, Program and Abstract, Lithoprobe Secretariat, University of
British Columbia, Vancouver, British Columbia, Lithoprobe Report No. 86, 4p.
Carville D.P, Leckie J.F, Moorhead C.F, Rayner J.G, Durbin A.A., 1990. Coronation Hill
gold-platinum palladium deposit: in Hughes FE editor. ‘Geology of the mineral
deposits of Australia and Papua New Guinea. The Australasian Institute of
Mining and Metallurgy Monograph 14, 759 – 762.
Carville D.P, Leckie J.F, Moorhead C.F, Rayner, J.G., 1991. Coronation Hill Unconformity
related gold, platinum, palladium prospect, Northern Territory. World Gold 91,
Australasian Institute of Mining and Metallurgy, 287-291.
Cathelineau, M., 1988. Cation site occupancy in Chlorite and illites as a function of
temperature: Clay Minerals, v. 23, p. 471–485.
Chacko, T., De, S. K., Creaser, R. A., Muehlenbachs, K., 2000. Tectonic setting of the
Taltson magmatic zone at 1.9–2.0 Ga: a granitoid-based perspective. Canadian
Journal of Earth Sciences 37, 1597–1609.
Chiarenzelli, J.R., Aspler, L.B., Villeneuve, M., Lewry, J.F., 1998. Paleoproterozoic
evolution of the Saskatchewan Craton, Trans-Hudson Orogen. J. Geol. 106, 247–
267.
Chipley, D., Paul A., Polito, T., Kyser K., 2007. Measurement of U-Pb ages of uraninite
and davidite by laser ablation-HR-ICP-MS. American Mineralogist 92, 1925–
1935.
216

Cinelu, S. and Cuney, M., 2006, Sodic metasomatism and U–Zr mineralization: A model
based on the Kurupung batholith (Guyana): Abstract, Geochimica et
Cosmochimica Acta, v. 70, p. 103.
Clayton, R.N., and Mayeda, T.K., 1963. The use of bromine pentafluoride in the extraction
of oygen from oxides and silicates for isotopic analysis: Geochimica et
Cosmochimica Acta, v. 27, p. 43–52.
Clendenin, C.W., Charlesworth E.G., Maske S., 1988. Tectonic style and mechanism of
Early Proterozoic successor basin development, southern Africa. Tectonophysics
156, 275-291.
Cloutier J, Kyser K, Olivo G.R, Alexandre P., Halaburda J., 2009. The Millennium
Uranium Deposit, Athabasca Basin, Saskatchewan, Canada: An Atypical
Basement- Hosted Unconformity-Related Uranium Deposit: Economic Geology,
104, 815-840.
Cocks, L.R.M. and Torsvik, T.H., 2002. Earth Geography from 500 to 400 million years
ago: a faunal and palaeomagnetic review. Journal Geological Society London
159, 631-644.
Collins, C.B., Farquhar, R.M. and Russel, R.D., 1954. Isotopic constitution of radiogenic
leads and the measurements of geological time. Geological Society America 65,
1-22.
Condon M.A and Walpole B.P, 1955. Sedimentary environments as a control of uranium
mineralisation in the Katherine– Darwin region, Northern Territory. Bureau of
Mineral Resources, Australia, Report 24.
Connors K.A and Page R.W., 1995. Relationships between magmatism, metamorphism and
deformation in the western Mount Isa inlier, Australia. Precambrian Res 71:131–
153
Cooper, J.A., 1973. On the age of uranium mineralization at Nabarlek, N. T., Australia. J.
Geol. Soc. Australia 19, 483
Corrigan, D., Pehrsson, S., Wodicka, N., Kemp, E., 2009. The Paleoproterozoic Trans-
Hudson Orogen: a prototype of modern accretionary processes. Journal
Geological Society of London 327, 457-479.
Crick, I.H, Muir M.D, Needham R.S, Roarty M.J., 1980. The Geology and Mineralization
of the South Alligator Valley Mineral Field. In J. Ferguson and A. Goleby, Eds.,
Uranium in the Pine Creek Geosyncline, p. 273–285. Proceedings of the
International Atomic Energy Agency, Vienna
217

Cuney, M.L., 2005. World-class unconformity-related uranium deposits: key factors for
their genesis. In: Mao Jingwen & Bierlein FP eds., Mineral Deposit Research:
Meeting the Global Challenge. Proceedings of the Eighth Biennial SGA Meeting
2005, Beijing, August 18–21.
Cuney, M. and Kyser, K., 2008. Recent and not-so-recent developments in U deposits and
implications for exploration: Mineralogical Association of Canada, Short Course
Series Volume 39, 257 p.
Cuney, M., 2010. Evolution of Uranium Fractionation Processes through Time: Driving the
Secular Variation of Uranium Deposit Types: Economic Geology, v. 105, p. 553-
569.
Dahlkamp, F.J., 1978. Geologic appraisal of the Key Lake U-Ni deposits, northern
Saskatchewan: Economic Geology, v. 73, p. 1430-1449.
Dalziel, I.W.D., 1991. Pacific margins of Laurentia and East Antarctica–Australia as a
conjugate rift pair: Evidence and implications for an Eocambrian supercontinent:
Geology, v. 19, 598–601.
DeBaar, H.J.W., 1991. On cerium anomalies of the Saragasso Sea: Geochimica et
Cosmochimica Acta, v. 55, p, 2981-2983.
Deer, WA, Howie RA, Zussman J 1992. An introduction to the rock-forming minerals:
London, Longman, 696.
Dieng, S., Kyser, K., Godin, L., 2011. Tectonic setting, Fluid History and Genesis of
Uranium Mineralization in the Beaverlodge area, Saskatchewan, Canada:
Mineralogical Association of Canada, the Society of Economic Geologists and
the Society for Geology Applied to Mineral Deposits (GAC- MAC), May 25-27,
2011 Ottawa.
Du Letian, 1986. Granite-type U deposits of China. In: H. Fuchs: Vein Type U Deposits:
International Atomic Energy Agency, IAEA-TECDOC, v. 361, p. 377-393.
Dudar, J. S., 1960. The geology and mineralogy of the Verna uranium deposit,
Beaverlodge, Saskatchewan University of Michigan. Unpublished M.Sc thesis,
312 pages.
Dudás, F.Ő., Davidson, A., Bethune, K.M., 1994. Age of the Sudbury diabase dikes and
their metamorphism in the Grenville province. Radiogenic age and isotopic
studies. Geological Survey of Canada, Current Research 1994-F, 97-106.
Eisele, J. and Isachsen, C.E., 2001. Crustal growth in southern Arizona: U-Pb
geochronologic and Sm-Nd isotopic evidence for addition of the
218

Paleoproterozoic Cochise block to the Mazatzal province. American Journal of
Earth Sciences 310, 773–797.
Eckelman, N.N. and Kulp J. L., 1957. Uranium-lead method of age determination II: North
American Localities. BuIletin G.S.A.
Edgecombe, S.M, Hazell M, Page R.W, Black L.P., Sun S.S., 2002. OZCHRON National
Geochronology Database Canberra: Geoscience Australia. Accessible at
http://www.ga.gov.au/ databases/20010926_27.jsp
Ernst, R.E. and Buchan, K.L., 2001a. Mantle Plumes: Their Identification through Time.
Geological Society of America Special Paper 352, 483-575.
Ernst, R.E and Buchan, K.L., 2001b. Large mafic magmatic events through time and links
to mantle plume heads. Geological Society of America Special Paper 362. 230 p
Ernst, R.E., 2007. Large igneous provinces in Canada through time and their metallogenic
potential, in: Goodfellow, W.D., ed., Mineral Deposits of Canada: A Synthesis of
Major Deposit-Types, District Metallogeny, the Evolution of Geological
provinces and Exploration Methods. Geological Association of Canada, Mineral
Deposits Division, Special Publication No. 5, 929-937.
Ernst, R.E., Wingate, M.T.D., Buchan, K.L., Li, Z.X., 2008. Global record of 1600–700 Ma
Large Igneous provinces (LIPs): implications for the reconstruction of the
proposed Nuna (Columbia) and Rodinia supercontinents. Precambrian Research
160, 159–178.
Eupene, G.S., 2003. Modelling of the Coronation Hill drill hole database. Northern
Territory Geological Survey, Technical Note 2003-011.
Evans, D.A.D. and Pisarevsky, S.A., 2008. Plate tectonics on early Earth Weighing the
paleomagnetic evidence: In Condie, K.C., Pease, V. (Eds.), When Did Plate
Tectonics Begin on Earth Geological Society of America, Special Paper, 249–
263.
Evans, A.D., Mitchell, R. N., Kilian, M., Joseph E. P., 2010. Reconstruction of Nuna: A
working hypothesis: GeoCanada 2010, 10-14 May, Calgary, Canada.
Evoy, E.F., 1961. Geology of the Gunnar uranium deposit, Beaverlodge area,
Saskatchewan: Unpublished Ph.D thesis, University of Wisconsin, Madison, 62
p.
Faure, G., 1989, Principles of Isotope Geology: Wiley, New York, 1986; Mir, Moscow.
Fayek, M. and Kyser, K., 1997. Characterization of multiple fluid-flow events and rareearth
elements mobility associated with formation of unconformity uranium
219

deposits in the Athabasca Basin, Saskatchewan: The Canadian Mineralogist 35,
627-658.
Ferenczi, P.A and Sweet I.P., 2005. Mount Evelyn, Northern Territory Second Edition.
1:250 000 geological map series explanatory notes, SD 53-05. Northern Territory
Geological Survey, Darwin.
Ferguson, J. and Needham R.S., 1978. The Zamu Dolerite. A Lower Proterozoic
preorogenic continental tholeiitic suite from the Northern Territory, Australia. J.
Geol. Soc. Aust, 25: 309-322.
Ferguson, J, Chappell B.W, Goleby A.B., 1980a. Granitoids in the Pine Creek Geosyncline:
in Ferguson J and Goleby AB editors. Uranium in the Pine Creek Geosyncline.
International Atomic Energy Agency, Vienna, 73–90.
Fisher, W.J., 1969. Mining practice in the South Alligator Valley: Atomic Energy in
Australia. 12, 25-40.
Foy, M.F., 1975. South Alligator Valley Uranium Deposits. In Knight, C. L. ed.., Geology
of Australia and Papua New Guinea: Melbourne, Australasian Institute of Mining
and Metallurgy, 1, 301–303.
Friedmann, J.S, and Grotzinger, P.J., 1994. Sedimentology, stratigraphy, and tectonic
implication of a Paleoproterozoic continental extensional basin: the El Sherana–
Edith River groups, Northern Territory, Australian: Canadian Journal of Earth
Sciences, 31, 743–764.
Fullerton, D.S., Colton, R.B., Bush, C.A. & Straub, A.W., 2003. Spatial and temporal
relationships of Laurentide continental glaciations and mountains glaciations on
the northern Plains in Montana and northwestern North Dakota, with
implications for reconstruction of the configurations of vanished ice sheets: U.S.
Geological Survey Miscellaneous Geologic Investigations Map, with text.
Gaál, G and Gorbatschev, R., 1987. An outline of the Precambrian evolution of the Baltic
Shield. In: Gaál, G and Gorbatschev, R. (Eds.), Precambrian Geology and
Evolution of the Central Baltic Shield. Special Issue. Precambrian Research 35:
15–52.Gao, S. and Wedepohl, K. H., 1995, The negative Eu anomaly in Archean
sedimentary rocks: Implications for decomposition, age and importance of their
granitic sources: Earth and Planetary Science Letters, v. 133, p. 81–94.
Ghandi, 2007. Significant Unconformity Associated Uranium Deposits of the Athabasca
Basin, Saskatchewan and Alberta, and Selected Related Deposits of Canada and
the World: Geological Survey of Canada, Open File 5005, Saskatchewan
Industry and Resources, Open File 2007- 11, CD-ROM.
220

Gibbs, A.K., and Olszewski, W.J., 1982, Zircon U-Pb ages of Guyana greenstone-gneiss
terrane: Precambrian Research, v. 17, p. 199–214.
Greenhalgh, D. and Jeffery P.N., 1959. A contribution to the Precambrian chronology of
Australia. Geochim. Cosmochim. Acta, 16: 39-57.
Gulson,, B.L. and Mizon K.J., 1980. Pb isotope studies at Jabiluka. In: Ferguson J and
Goleby, AB Eds.., Proceedings of the International Uranium Symposium on the
Pine Creek Geosyncline International Atomic Energy, Vienna, 439–455.
Gustafson, L.B. and Curtis L.W., 1983. Post-Kombolgie metasomatism at Jabiluka,
Northern Territory, Australia, and its significance in the formation of high-grade
uranium mineralization in lower Proterozoic rocks. Economic Geology 78, 26–
56.
Gorbatschev, R., and Bogdanova, S. 1993. Frontiers in the Baltic Shield: Precambrian
Research, v. 64, pp. 3–21.
Hajnal, Z., Lucas, S.B., White, D.J., Lewry, J., Bezdan, S., Stauffer, M.R. & Thomas,
M.D., 1996. Seismic reflection images of strike-slip faults and linked
detachments in the Trans-Hudson Orogen, Tectonics, 15, 427-439.
Hand, M., 2006. Intracratonic Orogeny in Mesoproterozoic Australia. In: LYONS, P. &
HUSTON, D. L. eds. Evolution and Metallogenesis of the North Australian
Craton. Geoscience Australia, Record2006/16, Alice Springs.
Hanley, L.M. and Wingate M.T.D., 2000. SHRIMP zircon age for an Early Cambrian
dolerite dyke: an intrusive phase of the Antrim Plateau Volcanics of northern
Australia: Australian Journal of Earth Sciences, 47, 1029–1040.
Hanmer, S., Williams, M.L., Kopf, C., 1995. Striding-Athabasca mylonite zone:
implications for Archean and Early Proterozoic tectonics of the western
Canadian shield: Canada Journal Earth Science 32, 178–196.
Harlan, S.S., Heaman, L.W., LeCheminant, A.N., Premo, W. R., 2003b. The Gunbarrel
mafic magmatic event: A key 780 Ma time marker for Rodinia plate
reconstructions. Geology 31, 1053–1056.
Hartlaub, R. P. and Ashton, K. E., 1998. Geological investigations of the Murmac Bay
group, Lake Athabasca north shore transect. Saskatchewan Geological Survey
Miscellaneous Report 98-4, 17–28.
Hartlaub, R. P., Heaman, L. M., Ashton, K. E., Chacko, T., 2004a. The Archean Murmac
Bay Group: evidence for a giant Archean rift in the Rae province, Canada.
Precambrian Research 131, 345–372.
221

Hartlaub, R.P., Heaman, L.M., Chacko, T., Ashton, K.E., 2007. Circa 2.3-Ga magmatism
of the Arrowsmith Orogen, Uranium City region, western Churchill Craton,
Canada. Journal of Geology 115, 181-195.
Hatcher, Jr., R.D., 2002. Alleghanian (Appalachian) Orogen, a product of zipper tectonics:
Rotational transpressive continent–continent collision and closing of ancient
oceans along irregular margins. Geological Society of America 364, 199-208.
Heaman, L.M., LeCheminant, A.N., Rainbird, R.H., 1992. Nature and timing of Franklin
igneous events, Canada; the break-up of Laurentia. Earth Planet Science Letters
109, 117–131.
Heaman, L.M., Hartlaub, R.P., Ashton, K.E., Harper, C.T., Maxeiner, R.O., 2003.
Preliminary results of the 2002–2003 Saskatchewan Industry and Resources
geochronology program. In Summary of Investigations 2003, 2. Saskatchewan
Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report
2003-4, 2, Paper A-3, p. 4.
Hedges, M.M., Wall V.J, Bloom M.S., 1984. Hydrothermal transport and deposition of
uranium: Modelling and implications. Geol. Soc. Australia, 12, 226-227.
Henderson, J.B., McGrath, P.H., Theriault, R.J., van Breemen, O., 1990. Intracratonic
indentation of the Archean Slave province into the early Proterozoic Thelon
tectonic zone of the Churchill province, NW Canadian shield: Canada Journal
Earth Science 27, 1699-1713.
Hendry, H. E., 1983. Sedimentology study of the Martin Group: In Summary of
Investigations, 1983, Saskatchewan Geological Survey, Miscellaneous Report
83-4, 46-48.
Hiatt, E.E. and Kyser T.K., 2000. Links between depositional and diagenetic processes in
basin analysis: Porosity and permeability evolution in sedimentary rocks:
Mineralogical Association of Canada Short Course, 28, 63–92
Hiatt, E.E, Fayek M, Kyser T.K, Polito 2001. The importance of early quartz cementation
events in the evolution of aquifer properties of ancient sandstones: Isotopic
evidence from ion probe analysis of sandstones from the McArthur, Athabasca,
and Thelon basins [abs]: Geological Society of America Abstracts with
Programs, 33, no 6, A74
Hiatt, E.E, Kyser T.K, Fayek M, Polito P, Holk G.J., Riciputi L.R., 2007. Early quartz
cements and evolution of paleohydraulic properties of basal sandstones in three
Paleoproterozoic continental basins: Evidence from in situ δ18O analysis of
quartz cements: Chemical Geology, 238, 19-37
222

Hills, J.H and Richards J.R., 1972. The age of uranium mineralization in northern Australia
Search; 392396
Hills, J.H. and Richards J.R., 1976. Pitchblende and galena ages in the Alligator Rivers
region, Northern Territory, Australia Mineralium Deposita, 11, 133–154
Hoeve, J., 1982, Perspective on U mineralization at Beaverlodge: Saskatchewan Research
Council, Publication. No. G-745-1-E-82.
Hoeve, J., and Quirt, D., 1984. U mineralization and host rock alteration in relation to clay
mineral diagenesis and evolution of the Middle-Proterozoic Athabasca basin,
Saskatchewan Canada: Saskatchewan Research Council, Publication, R-855-2-B,
190 p.
Hoffman, P.F., 1987. Continental transform tectonics: Great Slave Lake shear zone (ca. 1.9
Ga), northwest Canada. Geology 15, 785-788.
Hoffman, P.F., 1988. United plates of America, the birth of a craton: early Proterozoic
assembly and growth of Laurentia. Annual Review of Earth and Planetary
Sciences 16, 543–603.
Hoffman, P.F., 1989. Precambrian geology and tectonic history of North America, in: The
Geology of North America: An Overview (eds. A.W. Bally and A.R. Palmer)
Geological Society of America, Boulder pp. 447-511.
Hoffman, P.F., 1990. Subdivision of the Churchill province and extent of the Trans-
Hudson Orogen, in: The Early Proterozoic Trans-Hudson Orogen of North
America. Edited by J.F. Lewry and M.R. Stauffer. Geology Association of
Canada, Special Paper, 37, 15-39.
Hoffman, P.F., 1997. Tectonic genealogy of North America, in: van der Pluijm, B,A. and
Marshak, S., eds., Earth structure: An introduction to structural geology and
tectonics: New York, McGraw-Hill, pp. 459–464.
Hou, G., Santosh, M., Qian, X., Lister, G.S., Li, J., 2008. Configuration of the late
Paleoproterozoic supercontinent Columbia: insights from radiating mafic dike
swarms. Gondwana Research 14, 395–409.
Hu, G.X., Clayton R.N., 2003. Oxygen isotope salt effects at high pressure and high
temperature and the calibration of oxygen isotope geothermometry: Geochimica
et Cosmochimica Acta v. 67, p. 3227-3246.
Hunter, R.C., Bethune, K.M., Ashton, K.E., 2003. Stratigraphic and structural
investigations of the Paleoproterozoic Thluicho Lake Group, central Zemlak
Domain (Uranium City Project). In: Summary of Investigations 2003, Volume 2,
223

Saskatchewan Geological Survey, Sask. Industry Resources, Misc. Rep. 2003-
4.2, CD-ROM, Paper A-2, p. 14.
Hunter, R.C., Bethune, K.M., Yeo, G.M., Ashton, K.E., 2004. Investigations of the
Thluicho Lake Group: A stratigraphic, structural and tectonic perspective
(Uranium City Project). In: Summary of Investigations 2004, Volume 2,
Saskatchewan Geological Survey, Sask. Industry Resources, Misc. Rep. 2004-
4.2, CD-ROM, Paper A-9, p. 14.
Hynes, A., 1980. Carbonatization and mobility of Ti, Y, and Zr in Ascot Formation
metabasalts, SE Quebec: Contrib. Miner. Petrol., v. 75, p. 79-87.
Jagodzinski E.A., 1991. Stratigraphy of the Pul Pul Rhyolite, South Alligator Valley
Mineral Field BMR Research Newsletter, 14, 4-5
Jagodzinski, E.A., 1992. A study of the felsic volcanic succession south-east of Coronation
Hill: Palaevolcanology-geochemistry-geochronology Bureau of Mineral
Resources, Geology and Geophysics, Record, 1992/9, 147
Jagodzinski, E.A., 1998. Shrimp U-Pb dating of ignimbrites in the Pul Pul Rhyolite,
Northern Territory AGSO Research Newsletter, 28, 23–25
Jefferson, C.W., Thomas, D.J., Gandhi, S.S., Ramaekers, P., Delaney, G., Brisbin, D.,
Cutts, C., Portella, P., and Olson, R.A., 2007, Unconformity-associated uranium
deposits of the Athabasca Basin, Saskatchewan and Alberta, in Jefferson, C.W.
and Delaney, G., eds., EXTECH IV: Geology and uranium EXploration
TECHnology of the Proterozoic Athabasca Basin, Saskatchewan and Alberta:
Geological Survey of Canada, Bulletin 588, p. 23-67.
Johns, R.W., 1970. The Athabasca U deposits: Western miner, Oct., p. 42-52
Johnston, J.D., 1984. Structural evolution of the Pine Creek inliers and mineralization
therein PhD thesis, Monash University, Australia
Joubin, F.R., 1955. Some economic U deposits in Canada. Precambrian Research , v. 28,
no.1 p. 6-8
Kamo, S. L., Gower, C. F., Krogh, T. E., 1989. Birthdate for the Iapetus Ocean A precise
U-Pb zircon and baddeleyite age for the Long Range dikes, southern Labrador:
Geology, v. 17, p. 602–605.
Karlstrom, K.E., Harlan, S.S., Williams, M.L., McLelland, J., Geissman, J.W. and Ahall,
K.I., 1999. Refining Rodinia: Geologic evidence for the Australia–Western U.S.
connection for the Proterozoic: GSA Today 9, no. 10, 1–7.
224

Karlstrom, E.T., 2000. Fabric and origin of multiple diamictons within the pre-Illinoian
Kennedy Drift of Waterton- Glacier International Peace Park, Alberta, Canada
and Montana, USA. Geological Society of America Bulletin, 112, 1496–1506.
Karlstrom, K.E., Ahall, K.-I., Harlan, S.S., William, M.L., McLelland, J. and Geissman,
J.W., 2001. Long-lived (1.8–0.8 Ga) convergent Orogen in southern Laurentia,
its extensions to Australia and Baltica and implications for refining Rodinia:
Precambrian Research 111, 5–30.
Koeppel, V., 1969. Age and history of the uranium mineralization of the Beaverlodge area,
Saskatchewan. Geological Survey Canada, paper 67-31, 111p.
Kojima, S., Takeda S., Kogita S., 1994, Chemical factors controlling the solubility of
uraninite and their significance in the genesis of unconformity-related U
deposits: Mineralium Deposita, v. 29 (4): p. 353-360.
Kotzer, T.G. and Kyser, T.K., 1993. O, U, and Pb isotopic and chemical variations in
uraninite: implications for determining the temporal and fluid history of ancient
terrains. Am. Mineral. 78, 1262-1274.
Kotzer, T.G., and Kyser, T.K., 1995. Petrogenesis of the Proterozoic Athabasca basin,
northern Saskatchewan, and its relation to diagenesis, hydrothermal U
mineralization and paleohydrology: Chemical Geology, v. 120, p. 45–89.
Kretz, R., 1983. Symbols for rock-forming minerals, American Mineralogist 68, 277-279.
Krupicka, J. and Sassano, G.P., 1972. Multiple deformations of crystalline rocks in the
Tazin Group, Eldorado, Fay Mine, NW Saskatchewan: Canadian Journal Earth
Science 9, 422-433.
Kyser, T.K., and Kerrich, R., 1991. Retrograde exchange of hydrogen isotopes between
hydrous minerals and water at low temperatures, in Taylor, Jr., H.P., O’Neil,
J.R., and Kaplan, I., 19 8 eds., Stable isotope geochemistry: A tribute to Samuel
Epstein: Geochemical Society Special Publication, v. 3, p. 409-424.
Kyser, T.K., Hiatt, E.E., Renac, C., Durocher, K., Holk, G., Deckart, K., 2000. Diagenetic
fluids in Paleo- and Meso-Proterozoic sedimentary basins and their implications
for long protracted fluid histories: In Fluids and Basin Evolution (T.K. Kyser,
ed.). Mineralogy Association Canada, Short Course, v. 28, p. 225-262.
Kyser, T.K., Polito, P.A., Holk, G.J. and Hiatt, E.E., 2003. Pb-isotope ratios in sandstones
near unconformity-related U deposits in Australia - a guide for exploration:
Association of Exploration Geochemists' 21st International Geochemical
Exploration Symposium, Dublin, Ireland, p. 75.
225

Kyser, K., and Cuney, M., 2008. Geochemical characteristics of U and analytical
methodologies, in Cuney, M. and Kyser, K., eds., Recent and not-so-recent
developments in U deposits and implications for exploration: Mineralogical
Association of Canada Short Course, v. 39, p. 23-85.
Labrenze, M.E. and Karlstrom, K.E., 1991. Timing of the Mazatzal Orogeny: Constraints
from the Young Granite, Pleasant Valley, Arizona, in: Karlstrom, K.E. and
DeWitt, E., (Eds.), Proterozoic geology and ore deposits of Arizona. Arizona
Geological Society Digest, v. 19, pp. 225–236.
Lally, J. and Worden K., 2004. Geochronology in the Pine Creek Orogen – new results
from NTGS: in ‘Annual Geoscience Exploration Seminar AGES. 2004 Record of
abstracts’ Northern Territory Geological Survey, Record 2004-001, 3–4
Lally, J.H. and Bajwah Z.U., 2006. Uranium deposits of the Northern Territory Northern
Territory Geological Survey, Report 20
Langford, F.F., 1981. The Martin Group in the Greater Beaverlodge area. In Summary of
Investigations 1981. Saskatchewan Geological Survey, Saskatchewan Energy
Mines, Miscellaneous Report 81-4, 38–43.
Langmuir, D., 1978. U solution-minral equilibria at low temperatures with applications to
sedimentary ore deposits: Geochimica et Cosmochimica Acta, v. 42, p. 547-569.
LeCheminant, A.N. and Heaman, L.M., 1989. Mackenzie igneous events, Canada: Middle
Proterozoic hotspot magmatism associated with ocean opening. Earth and
Planetary Science Letters 96, 38–48.
LeCheminant, A.N. and Heaman, L.M., 1994. 779 mafic magmatism in the northwestern
Canadian shield and northern Cordillera: A new regional time-marker. Eighth
International Conference on Geochronology, Cosmochronology and Isotope
Geology, Berkeley, California, Programs with Abstract: U.S. Geological Survey
Circular 1107, 187 p.
LeCheminant, A.N., Buchan, K.L., van Breemen, O., 1997. Paleoproterozoic continental
breakup and reassembly: Evidence from 2.19 Ga diabase dike swarms in the
Slave and western Churchill provinces, Canada: Geological Association of
Canada/Mineralogical Association of Canada, Abstract volume, p. A-86.
Leroy, J., 1978, The Margnac and Fanay U deposits of the La Crouzille district (western
Massif Central, France), geologic and fluid inclusion studies: Economic
Geology, v. 73, p. 1611-1634.
Lewry, J.F. and Collerson, K.D., 1989. The Trans-Hudson Orogen: Extent, subdivision and
problems, in: The Early Proterozoic Trans-Hudson Orogen of North America.
226

Edited by J.F. Lewry and M.R. Stauffer. Geological Association of Canada,
Special Paper 37, 1-14.
Li, Z.X. Bogdanova, S.V., Collins, A.S., Davidson, A. B., Wael, D., Ernst, R.E.,
Fitzsimons, I.C.W., Fuck , R.A., Gladkochub, D.P., Karlstrom, K.E., Natapovm,
S. L. L.M., Peas, V., Pisarevsky , S.A. Thrane , K., Vernikovsky, V., 2008.
Assembly, configuration, and break-up history of Rodinia: a synthesis.
Precambrian Research 160, 179–210.
Ludwig, K.R, Grauch R.I, Nutt C.J, Frisman D, Nash JT, Simmons K.R., 1985. Age of
uranium ores at Ranger and Jabiluka unconformity vein deposits, Northern
Territory, Australia Economic Geology 82, 857–874
Ludwig, K.R, Frauch, R.I, Nutt, C.J, Frishman, D, Simmons K.R., 1987. Age of uranium
mineralization at the Jabiluka and Ranger deposits, Northern Territory, Australia:
new U-Pb isotope evidence: Economic Geology, 82, 857–874
Ludwig, K.R., 2000. Decay constant errors in U–Pb concordia-intercept ages. Chem. Geol.
166, 315–318.
Maas, R., 1989. Nd-Sr isotope constraints on the age and origin of unconformity type
uranium deposits in the Alligator Rivers Uranium Field, Northern Territory,
Australia Economic Geology 84, 64–90
MacCready, T, Goleby B.R, Goncharov A, Drummond B.J, Lister G.S., 1998. A
framework of overprinting orogens based on interpretation of the Mount Isa deep
seismic transect: Economic Geology, 93, 1422–1434
Macdonald, R. and Slimmon, W.L., 1985. Bedrock Geology of the Greater Beaverlodge
Area, NTS 74N-6 to -11: Saskatchewan Energy Mines, Map 241A, 1:100 000
scale.
Marumo, K., Nagasawa K., Kuroda Y., 1980. Mineralogy and hydrogen isotope
geochemistry of clay minerals in the Ohnuma geothermal area, northeastern
Japan: Earth and Planetary Science Letters, v. 47, p. 255–262.
Mazimhaka, P.K. and Hendry, H.E., 1984. The Martin Group, Beaverlodge Area. In
Summary of Investigations 1984, Saskatchewan Geological Survey,
Saskatchewan Energy Mines, Miscellaneous Report 84-4, 53-62.
Mazimhaka, P.K. and Hendry, H.E., 1985. The Martin Group, Charlot Point and Jug Bay
areas. In Summary of Investigations 1985. Saskatchewan Geological Survey,
Saskatchewan Energy Mines, Miscellaneous Report 85-4, 67-80.
McDonough, M. R. McNicoll, V. J. Schetsela, E. M., Grover, T. W., 2000.
Geochronological and kinematic constraints on crustal shortening and escape in a
227

two-sided oblique-slip collisional and magmatic Orogen, Paleoproterozoic
Taltson magmatic zone, northeastern Alberta: Canada Journal of Earth Science
37, 1549–1573.
McDonough, W. F. and Sun, S, S., 1995. The composition of the Earth: Chemical Geology,
v. 120, p. 223–253.
McLelland, J., Daly, S., McLelland, J., 1996. The Grenville orogenic cycle: An Adirondack
perspective. Tectonophysics, 265, 1-29.
Mckenzie, D. P., 1978. Some remarks on the development of sedimentary basins. Earth and
Planetary Science Letters 40, 25-32.
McNicoll, V.J., Thériault, R.J., McDonough, M.R., 2000. Taltson basement gneissic rocks;
U–Pb and Nd isotopic constraints on the basement to the Paleoproterozoic
Taltson magmatic zone, northeastern Alberta: Canada Journal of Earth Science
37, 1575-1596.
Mercadier, J., Cuney, M., Lach, P., Boiron, M.C., Bonhoure, J., Richard, A., Leisen, M.,
Kister, P., 2011. Origin of uranium deposits revealed by their rare earth element
signature: Terra Nova, v. 23, p. 264-269.
Metcalfe, I., 2001. Paleozoic and Mesozoic tectonic evolution and biogeography of SE
Asia-Australasia Pages 15–34 in I Metcalfe, JMB Smith, M Morwood, and I
Davidson, eds, Faunal and Floral Migrations and Evolution in SE Asia-
Australasia AA Balkema, Lisse, Switzerland
Mernagh, T.P, Heinrich C.A, Leckie J.F, Carville D.P, Gilbert D.J, Valenta R.K, Wyborn
L.A.O., 1994. Chemistry of low-temperature hydrothermal gold, platinum, and
palladium±uranium. mineralization at Coronation Hill, Northern Territory,
Australia: Economic Geology, 89, 1053–1073
Mernagh T.P and Wyborn L.A.I., 1994. The genesis of the Coronation Hill gold, palladium
and platinum deposit: implications for exploration: in Australian research on ore
genesis symposium, Adelaide, South Australia, December 12 -14, 1994,
Proceedings Australian Mineral Foundation, Adelaide, 231 – 235
Miller, J. A., Buick, I. S., Cartwright, I., 2002. Fluid processes during the exhumation of
high-P metamorphic belts, Mineral. Mag. 66, 93-119.
Miller, J.A. and Cartwright, I., 2006. Albite vein formation during exhumation of highpressure
terranes: a case study from Alpine Corsica. Journal of Metamorphic
Geology, 24, 409-428.
228

Molnar, P. and Atwater. T., 1978. Interarc spreading and Cordilleran tectonics as alternates
related to the age of subducted oceanic lithosphere: Earth and Planetary Science
Letters 41, 330-340.
Moores, E.M., 1991. The Southwest U.S.–East Antarctica (SWEAT) connection: A
hypothesis. Geology 19, 425–428.
Morelli, R., Ashton, K., Ansdell, K., 2001. A geochemical investigation of the Martin
Group igneous rocks, Beaverlodge Domain, northwestern Saskatchewan. In
Summary of Investigations 2001, Saskatchewan Geological Survey,
Saskatchewan Energy Mines v. 2, Miscellaneous Report 2001-4, 64-75.
Morelli, R.M., Hartlaub, R.P., Ashton, K.E., Ansdell, K.M., 2009. Evidence for enrichment
of subcontinental lithospheric mantle from Paleoproterozoic intracratonic
magmas: geochemistry and U–Pb geochronology of Martin Group igneous rocks,
western Rae craton, Canada. Precambrian Research 175, 1-15.
Morton, R. D. and Sassano, G. P., 1972. Structural studies on the uranium deposit of the
Fay Mine, Eldorado, northwest Saskatchewan. Canada Journal of Earth Science
9, 803-823.
Mountain, B.W. and Wood S.A., 1988a. Solubility and transport of platinum-group
elements in hydrothermal solutions: Thermodynamic and physical chemical
constraints; in Geo-Platinum 87, Prichard, HM, Potts, PJ, Bowles, JFW and
Cribb, SJ eds., Elsevier Science Publishing Ltd, Barking, Essex, UK, 57-82
Mountain, B.W. and Wood S.A., 1988b. Chemical controls on the solubility, transport, and
deposition of platinum and palladium in hydrothermal solutions: A
thermodynamic approach; Economic Geology 83, 492-510
Müller, R.D, Gaina C, Clarke S., 2000. Seafloor spreading around Australia, In: J Veevers
ed., Billion-year earth history of Australia and neighbours in Gondwanaland –
BYEHA 18-28
Myers, J.S, Shaw R.D, Tyler I.M., 1996. Tectonic evolution of Proterozoic Australia
Tectonics 15, 1431 – 1446
Needham, R.S, Crick I.H, Stuart-Smith P.G., 1980. Regional geology of the Pine Creek
Geosyncline: in Ferguson J and Goleby AB editors. Uranium in the Pine Creek
Geosyncline International Atomic Energy Agency, Vienna, 1-22
Needham, R.S., 1982. Cahill, Northern Territory 1:100 000 geological map series
commentary, 5472 Bureau of Mineral Resources, Australia
Needham, R.S. and Stuart-Smith P.G., 1984. The relationship between mineralisation and
depositional environment in the Early Proterozoic metasediments of the Pine
229

Creek Geosyncline: in ‘The mineral potential of northern Australia and changing
concepts of development’ Australasian Institute of Mining and Metallurgy, 1984
Annual Conference, Darwin, Northern Territory, Australia, August 1984
Australasian Institute of Mining and Metallurgy, Conference Series 13, 201–211
Needham, R.S. and Stuart-Smith P.G., 1985. Stratigraphy and tectonics of the Early to
Middle Proterozoic transition, Katherine-E1 Sherana area, NT Aust J Earth Sci,
32: 219-230
Needham, R.S. and Stuart-Smith P.G., 1986. Coronation Hill U-Au mine, South Alligator
Valley, Northern Territory: an epigenetic sandstone-type deposit hosted by
debris-flow conglomerate BMR Journal of Australian Geology and Geophysics
10, 121-131
Needham, R.S., 1987. A review of mineralisation in the South Alligator Conservation Zone
Bureau of Mineral Resources, Australia, Record 1987/52
Needham, R.S., 1987. Geology of the Alligator Rivers Uranium Field, northern Territory
Australian Government Publishing Service, Canberra
Needham, R.S, Stuart-Smith P.G, Page R.W., 1988. Tectonic evolution of the Pine Creek
Inlier, Northern Territory Precambrian Research 40/41, 543–564
Needham, R.S., 1988a. Geology of the Alligator Rivers Uranium Field, Northern Territory
Bureau of Mineral Resources, Australia, Bulletin 224
Needham, R.S., 1988b. Geology and mineralization of the South Alligator Valley Mineral
Field 1:75 000 scale map. Bureau of Mineral Resources, Australia
Needham, R.S. and DeRoss G.J., 1990. Pine Creek Inlier – regional geology and
mineralisation: in Hughes FE editor. ‘Geology and mineral deposits of Australia
and Papua New Guinea’ Australasian Institute of Mining and Metallurgy,
Monograph 14, 727–737
Neumann, N.L. and Fraser G.L., 2007. Geochronological synthesis and Time-Space plots
for Proterozoic Australia Geoscience Australia Record 2007/06
O’Hanley, D.S., Kyser, T.K., Sibbald, T.I.I., 1991. The Age of the Mine Granites,
Goldfields Area. In Summary of Investigations, 1991; Saskatchewan Geological
Survey; Saskatchewan Energy and Mines, Miscellaneous Report 91-4.
Ohmoto, H. and Rye R. O., 1979. Isotopes of sulfur and carbon: In Geochemistry of
Hydrothermal Ore Deposits, 2nd ed. (ed. H. L. Barnes), p. 509–567.
Ojakangas, R.W., 1979. Sedimentation of the basal Kombolgie Formation Upper
Precambrian-Carpentarian. Northern Territory, Australia: Possible significance in
230

the genesis of the underlying Alligator Rivers Unconformity- type uranium
deposits US Dept of Energy, GJBX- 173 79., 38
O’Neil,, J..R. and Taylor H.P. Jr., 1969. Oxygen isotope equilibrium between muscovite
and water: Journal of Geophysical Research, 74, 6012–6022
Page, R.W, Compston W, Needham R.S., 1980. Geochronology and evolution of the late
Achaean basement and Proterozoic rocks in the Alligator River Uranium Field,
Northern Territory, Australia: in Ferguson J and Goleby AB editors. Uranium in
the Pine Creek Geosyncline International Atomic Energy Agency, Vienna, 39–68
Page, R.W. and Williams I.S., 1988. Age of the Barramundi Orogeny in northern Australia
by means of ion microprobe and conventional U-Pb zircon studies Precambrian
Research 40/41, 21–36
Page, R.W. and Bell T.H., 1986. Isotopic and structural responses of granite to successive
deformation and metamorphism J Geol 94:365–379
Persons, S.S., 1983. U–Pb geochronology of Precambrian rocks in the Beaverlodge area,
northwestern Saskatchewan: Unpublished M.Sc. Thesis, University of Kansas,
68 p.
Peiris, E. and Parslow, G., 1988. Geology and geochemistry of the uranium-gold
mineralization in the Nicholson Bay-Fish Hook Bay Area: In Summary of
Investigations, Saskatchewan Geological Survey Miscellaneous Report 88-4, p.
70-77
Pharaoh, T. C. and Brewer, T. S., 1990. Spatial and temporal diversity of Early Proterozoic
volcanic sequences. Comparisons between the Baltic and Laurentian Shields:
Precambrian Research, v. 47, p. 169-189.
Pietsch, B.A. and Stuart-Smith P.G., 1987. Darwin SD52-4 1:250 Geological Map Series,
Northern Territory Geological Survey, Department of Mines and Energy
Comparisons between the Baltic and Laurentian Shields: Precambrian Research,
v. 47, p. 169-189.
Pinheiro, S.S., Fernandes, P.E.C.A., Pereira, E.R., Vasconcelos, E.G., Pinto, A.C.,
Montalva˜o, R.M.G., Issler, R.S., Dall’Agnoll, R., Teixeira, W., and Fernandes,
C.A.C., 1976, Geologia, in Levantamento de Recursos Naturais, Projeto Radar na
Amazoˆnia: Rio de Janeiro, Brazil, Departamento Nacional da Produc¸a˜o
Mineral, sheet NA.19—Pico da Neblina, v. 11, p. 19–137.
Piper, J.D.A., 2000. The Neoproterozoic Supercontinent: Rodinia or Palaeopangaea: Earth
and Planetary Science Letters 176, 131-146.
231

Piper, J.D.A., 2004. Discussion on “The making and unmaking of a supercontinent:
Rodinia revisited” Tectonophysics, 375, 261–288.
Pisarevsky, S.A., Natapov, L.M., Donskaya, T.V., Gladkochub, D.P., Vernikovsky, V.A.,
2008. Proterozoic Siberia: a promontory of Rodinia. Precambrian Research 160,
66-76.
Plant, J.A., Simpson, P.R., Smith, B., Windley, B.F., 1999. U ore deposits: products of the
radioactive earth: Reviews in Mineralogy and Geochemistry, v. 38, p. 255-319.
Polito, P.A, Kyser T.K, Marlatt J, Alexandre P, Bajwah Z.U, Drever, D., 2004.
Significance of alteration assemblages for the origin and evolution of the
Proterozoic Nabarlek unconformity-related uranium deposit, Northern Territory,
Australia Economic Geology 99, 113–139
Polito, P.A, Kyser T.K, Thomas D, Marlatt J, Drever G., 2005. Re-evaluation of the
petrogenesis of the Proterozoic Jabiluka unconformity-related U deposit,
Northern Territory, Australia Miner Depos 40:257–288
Polito, P.A, Kyser T.K, Southgate P.N, Jackson M.J., 2006. Sandstone Diagenesis in the
Mount Isa Basin: An isotopic and fluid inclusion perspective in relation to
district-wide Zn, Pb, and Cu mineralization Econ Geol 101:1159–1188
Polito, P.A, Kyser K.T, Stanley C., 2007. The Proterozoic, albitite hosted, Valhalla U
deposit, Queensland, Australia: A description of the alteration assemblage
associated with U mineralization in diamond drill hole: Mineralium Deposita, 44,
p11–40
Porto da Silveira, C,L., Schorscher H,D., Miekeley N., 1991, The geochemistry of
albitization and related U mineralization, Espinharas, Paraiba (PB), Brazil.
Journal of Geochemical Exploration, v. 40, p. 329–347.
Quirt, D.H., 2003. Athabasca unconformity-type uranium deposits: one deposit type with
many variations, in Cuney, M., ed., Uranium Geochemistry 2003, International
Conference, April 13-162003, Proceedings: Unité Mixte de Recherche CNRS
7566 G2R, Université Henri Poincaré, Nancy, France, p. 309-312.
Rainbird, R.H., Stern, R.A., Rayner, N., Jefferson, C.W., 2007. Age, provenance and
regional correlation of the Athabasca Group, Saskatchewan and Alberta
constrained by igneous and detrital zircon geochronology, in: Jefferson, C.W.,
Delaney, G. (Eds.), Extech IV: Geology and Uranium Exploration Technology of
the Proterozoic Athabasca Basin Saskatchewan and Alberta. Geological Survey
of Canada, Bulletin 588, pp. 193-209.
232

Ramaekers, P., 1981. Hudsonian and Helikian basins of the Athabasca region, northern
Saskatchewan, in: Campbell, F.H.A. (Ed.), Proterozoic Basins of Canada.
Geological Survey of Canada, Paper 81-10, pp. 219-233.
Ramsay, J G., 1967. Folding and fracturing of rocks. New York: McGraw Hill. 568 p.
Rasmussen, B, Sheppard S, Fletcher I.R., 2006. Testing ore deposit models using in situ U-
Pb geochronology of hydrothermal monazite: Paleoproterozoic gold
mineralization in northern Australia Geology 34:77–80
Rees, M.I., 1992. History of the fluids associated with the Lode-Gold deposits, and
complex U-PGE-Au vein-typedeposits, Goldfields Peninsula, northern
Saskatchewan, Canada; unpubl. M.Sc. thesis, Univ. Saskatchewan, 209p.
Riley, G.H, Binns R.A, Craven,S.J., 1980. Rb-Sr chronology of micas at Jabiluka, In:
Ferguson, John, and Goleby, A B, eds, Uranium in the Pine Creek Geosyncline:
Vienna, Int Atomic Energy Agency, 457-468
Rivers, T., 1997. Lithotectonic elements of the Grenville province: Review and tectonic
implications. Precambrian Research 86, 117-154.
Robinson, S.C., 1955. Mineralogy of Uranium Deposits, Goldfields, Saskatchewan.
Canadian Geological Survey, Bulletin 31.
Rogers, J.J.W. and Santosh, M., 2002. Configuration of Columbia, a Mesoproterozoic
supercontinent: Gondwana Research 5, 5-22.
Romberger, S.B., 1984. Mechanisms of Deposition of Gold in Low Temperature
Hydrothermal Systems: Assoc Expl. Geochemists Annual Meeting, Reno,
Nevada.
Russel, R.D. and Ahren, L. D., 1957. Additional regularities among discordant Pb/U ages.
Geochimica et Cosmochimica Acta 11, 213-218.
Ruzicka, V.R., 1996. Unconformity-associated uranium, Chapter 7 in Eckstrand, O.R.,
Sinclair, W.D., and Thorpe, R.I., eds., Geology of Canadian Mineral Deposit
Types: Geological Survey of Canada, Geology of Canada, v, 8, p. 197-210.
Saltikoff, B., Puustinen, K. and Tontti, M., 2006. Metallogenic zones and metallic mineral
deposits in Finland–Explanation to the Metallogenic Map of Finland. Geological
Survey of Finland, Special paper 35, pp 66.
Santos, J.O.S., Hartmann, L.A., Gaudette, H.E., Groves, D.I., McNaughton, N.J., and
Fletcher, I.R., 2000. A new understanding of the provinces of the Amazon craton
based on integration of field mapping and UPb and Sm-Nd geochronology:
Gondwana Research, v. 3, p. 453–488. Science B.V., Amsterdam, 19–
233

99.Sheppard SMF and Gilg HA 1996. Stable isotope geochemistry of clay
minerals: Clay Minerals, 31, 1-24
Santos, J.O.S., Potter, P.E., Reis, N.J., Hartmann, L.A., Fletcher, I.R., McNaughton, N.J.,
2003. Age, source and regional stratigraphy of the Roraima Supergroup and
Roraima-like outliers in northern South America based on U-Pb geochronology.
Geological Society of America Bulletin 115 (3): 331–348.
Sassano, G. P., 1972. The nature and origin of the uranium mineralization at the Fay Mine,
Eldorado, Saskatchewan: Unpublished Ph.D. thesis, University of Alberta,
Edmonton, Alberta, 416p.
Sassano, G.P., Fritz P., Morton R.D., 1972. Paragenesis and isotopic composition of some
gangue minerals from the uranium deposits of Eldorado, Saskatchewan.
Canadian Journal of Earth Science 9, 141-157.
Sassano, G.P., Baadsgaard, H., Burwash, R.A., 1974. Rb-Src age of the late kinematic
phase of the Hudsonian Orogen in the Beaverlodge area, Saskatchewan:
Canadian Journal of Earth Science 11, 643-649.
Scott, B.P., 1978. The geology of an area east of Thluicho Lake, Saskatchewan (part of
NTS area 74N-11). Saskatchewan Mineral Resources, Report 167, p. 51
(1:31680 scale map).
Sener, A.K, Grainger C.J, Groves D.I., 2002. Epigenetic gold-platinum-group deposits:
examples from Brazil and Australia Transactions of the Institution of Mining and
Metallurgy: Section B 111: 65-73
Shergold, J.H. and Druce E.C., 1980. Upper Proterozoic and Lower Palaeozoic rocks of the
Georgina Basin In Henderson, RA & Stephenson, PJ Editors.: The Geology and
Geophysics of Northeastern Australia Geological Society of Australia,
Queensland Division, 149-174
Sibbald, T.I.I., 1982. Uranium Metallogenic Studies: Nicholson Bay Area. In Summary of
Investigations, 1982; Saskatchewan Geological Survey; Saskatchewan Energy
and Mines, Miscellaneous Report 82-4.
Sibbald, T.I.I., 1983. Geology of the crystalline basement, NEA/AEA Athabasca Test Area,
in: Cameron, E.M. (Ed.), Uranium Exploration in Athabasca Basin
Saskatchewan, Canada, Geological Survey of Canada, pp. 1-14.
Sibbald, T.I.I. and Quirt, D., 1987. U deposits of the Athabasca basin: Saskatchewan
Research Council Publication R-855-1-G-87, 79 p.
Sibson, RH., Moore, J., Rankin, A., 1975. Seismic pumping-a hydrothermal fluid transport
mechanism. Journal of Geological Society of London, vol. 131, p. 653-659.
234

Sibson, R.H., 1977. Fault rocks and fault mechanisms: Journal Geological Society, London
133, 191-213.
Sibson, R.H., 1987. Earthquake rupture as a hydrothermal mineralizing agent. Geology, vol
15, p. 701-704.
Simonen, A., 1986. Stratigraphic studies on the Precambrian in Finland. Geological Survey
of Finland, Bulletin 336: 21–37
Skirrow, R.G., Jaireth, S., Huston, D.L., Bastrakov, E.N., Schofield, A., van, der Wielen,
S.E., Barnicoat, A.C., 2009. U Mineral, Systems: Processes, Exploration Criteria
and a New Deposit Frame Systems: Framework; work; Geoscience Australia
Record 2009/20, 44 p.
Slater, J. R., 1983. Some relationships between deformation, mineralization and ore genesis
at the Fay mine, Eldorado, Saskatchewan: Unpublished M.Sc. thesis, University
of Alberta, 105 p.
Smellie, J.A.T. and Laurikko, J., 1984. Skuppesavon, northern Sweden: a U mineralization
associated with alkali metasomatism: Mineralium Deposita v. 19, p. 184-192.
Smith, D.K., 1984. U mineralogy. In: De Vivo B, Ippolito F, Capaldi G, Simpson PR (eds)
U geochemistry, mineralogy, geology, exploration and resources: The Institution
of Mining and Metallurgy, London, England, p 43–88.
Sorjonen-Ward, P., Claoué-Long, J. and Huhma, H., 1994. SHRIMP isotope studies of
granulite zircons and their relevance to early Proterozoic tectonics in northern
Fennoscandia. In: Lamphere, M., Darymple, G., Turrin, B (Eds.), Abstract of the
Eighth International Conference on Geochronology, Cosmochronology and
isotope Geology, Berkeley, Califormia, USA, June 5-11, 1994. U.S Geological
Survey Circular 1107: 1–299.
Sorjonen-Ward, P. & Luukkonen, E., 2005. Archean rocks. In: Lehtinen, M., Nurmi, P. A.
& Rämö, O. T., (eds.) Precambrian geology of Finland: key to the evolution of
the Fennoscandian Shield. Developments in Precambrian geology 14. Elsevier
Spikings, R.A, Foster D.A, Kohn B.P, Lister G.S., 2001. Post-orogenic

Proceedings Darwin Conference 1984 Australasian Institute of Mining &
Metallurgy; 329338
Stuart-Smith, P.G, Needham R.S, Page R.W, Wyborn L.A.I., 1993. Geology and mineral
deposits of the Cullen Mineral Field, Northern Territory Australian Geological
Survey Organisation, Bulletin 229
Sweet, I.P, Brakel A.T, Carson L., 1999. The Kombolgie Subgroup a new look at an old
formation AGSO Research Newsletter 1999; No 30: 2628
Taylor J., 1968. Origin and controls of uranium mineralization in the South Alligator
valley: in Berkman DA, Cuthbert RH and Harris LA Editors. Uranium in
Australia Symposium, Rum Jungle, June 1968 Proceedings Australasian Institute
of Mining and Metallurgy, 32-44
Taylor, H. P. Jr., 1974. The application of oxygen and hydrogen isotope studies to
problems of hydrothermal alteration and ore deposition. Economic Geology, v.
69, p. 843.
Thériault, R.J., 1992. Nd isotopic evolution of the Taltson magmatic zone, Northwest
Territories, Canada: insights into Early Proterozoic accretion along the western
margin of the Churchill province: Journal of Geology 100, 465–475.
Thompson, A.G. and Barnes, C.G., 1999. 1.4 Ga peraluminous granites in central New
Mexico: Petrology and geochemistry of the Priest pluton: Rocky Mountain.
Geology 34, 223–243.
Torsvik, T.H. and Van der Voo, R., 2002. Refining Gondwana and Pangaea
Palaeogeography: Estimates of Phanerozoic (octupole) non-dipole fields.
Geophysical Journal International 151, 771-794.
Tortosa, D. J.-J., 1983. The Geology of the Cenex Uranium Deposit, Beaverlodge,
Saskatchewan, in: C.I.M.M. Special Volume 33, Uranium Deposits of Canada,
Dr. E. L. Evans, Editor.
Tremblay, L. P., 1968. Geology of the Beaverlodge Mining Area, Saskatchewan (Parts of
74N/9 and 74N/10). Geological Survey of Canada, Memoir 367.
Tremblay, L.P., 1972. Geology of the Beaverlodge Mining Area, Saskatchewan. Geological
Survey of Canada, Memoir 367, including two maps at 1:14,400 that encompass
the entire Beaverlodge Mining Area, 265p.
Turek, A., 1962. Geology of the Cinch Lake Mine Limited, Uranium City, Saskatchewan.
Unpublished M.Sc. thesis, University of Alberta, 101 p.
236

Valenta, R.K., 1989. Structure and mineralization in the South Alligator Valley, NT Bureau
of Mineral Resources
Valenta, R.K., 1990. Structural setting of unconformity-related U Au platinoid
mineralization in the South Alligator Valley, NT In: Gondwana and Resources
Geologl Society of Australia; Abstracts No 25: 173
Valenta, R.K., 1991. Structural controls on mineralization of the Coronation Hill deposit
and surrounding area: Australia Bureau of Mineral Resources: Geology and
Geophysics Record1991/107, 186
Walpole, B.P, Crohn P.W, Dunn P.R, Randal M.A., 1968. Geology of the Katherine–
Darwin region, Northern Territory Bureau of Mineral Resources, Australia,
Bulletin 82
Warren, R.G. and Kamprad, J.L., 1990. Mineralogical petrographic and geochemical
studies in the South Alligator region Pine Creek inlier, NT: Australia Bureau of
Mineral Resources, Geology and Geophysics Record1 990/54, 113
Wasserburg, G. J. and Hayden, R. J., 1955. Ar 40 :K 40 dating. Geochimica et Cosmochimica
Acta 7, 51–60.
Wenner, D.B., and Taylor, H.P., Jr., 1971. Temperature of serpentinization of ultramafic
rocks based on O18/O16 fractionation between coexisting serpentinite and
magnesite: Contributions to Mineralogy and Petrology, v. 32, p. 165–185.
Whitmeyer, S. J. and Karlstrom K. E., 2007. Tectonic model for the Proterozoic growth of
North America. Geosphere, 3, 220–259.
Wiedenbeck, M., Allé P., Corfu, F., Griffin, W.L, Meier, M., Oberli, F., von Quadt, A.,
Roddick, J.C., Spiegel, W., 1995. Three natural Zircon standards for U-Th-Pb,
Lu-Hf, trace element and REE analysis: Geostandards Newsletter, v. 19, p. 1-23.
Wilde, A.R, Mernagh T.P, Bloom M.S, Hoffmann C.F., 1989. Fluid inclusion evidence on
the origin of some Australian Unconformity-related Uranium Deposits:
Economic Geology, 84, 1627- 1642
Wilde, A.R., 1992. Unconformity-related uranium-gold deposits on northern Australia;
resources, genesis and exploration IAEA-Tecdoc, 650, 49-58
Williams, H., Hoffman, P.F., Lewry, J.F., Monger, J.W.H., Rivers, T., 1991. Anatomy of
North America: thematic portrayals of the continent. Tectonophysics 187, 117–
134.
Wilson, M.R., and Kyser, K., 1987. Stable isotopes geochemistry of alteration associated
with the Key Lake U deposit, Canada: Economic Geology, v. 82, p. 1540–1557.
237

Wingate, M.T.D, Pisarevsky SA, Evans D.A.D., 2002. Rodinia connections between
Australia and Laurentia: no SWEAT, no AUSWUS Terra Nova 14:121–128
Wingate, M.T.D and Giddings J.W., 2000. Age and paleomagnetism of the Mundine Well
dyke swarm, Western Australia: implications for an Australia–Laurentia
connection at 755 Ma Precamb Res100:335–357
Wray, E.M, Ayres, D.E, Ibrahim H., 1985. Geology of the Mid-west uranium deposit
northern Saskatchewan Canadian Institute of Mining and Metallurgy, 32, 54-66
Wyborn, L.A.I, Valenta R, Needham R.S, Jagodzinski E.A, Whitaker A, Morse M.P., 1990.
A review of the geological, geophysical and geochemical data of the Kakadu
Conservation Zone: a basis for the assessing resource potential Report by the
Bureau of Mineral Resources to the Resource Assessment Commission, Inquiry
on the Kakadu Conservation Zone
Wyborn, L.A.I, Valenta, R.K, Jagodzinski, E.A, Whitaker A, Morse M.P, Needham R.S.,
1991. A review of the geological, geophysical and geochemical data of the
Kakaduc conservation zone basis for estimating resource potential: Australia
Bureau of Mineral Resources Geology and Geophysics Report to Resource
Assessment Commission 2, 90 p
Wyborn, L.A.I., 1992. Au-Pt-Pd-U mineralization in the Coronation Hill-EL Sherana
region NT: BMR Research Newsletter, 16, 1-3
Wyborn, L.A.I, Budd A., Bastrikova, I., 1997. The metallogenic potential of Australian
Proterozoic Granites Final Meeting Report Australian Geological Survey
Organisation, Canberra
Yeo, G.M., 2005. Stratigraphy and metallogeny of the Paleoproterozoic Thluicho Lake
Group, northwestern Saskatchewan (NTS 74N/11). In: Summary of
Investigations 2005, Volume 2, Saskatchewan Geological Survey, Sask. Industry
Resources, Misc. Rep. 2005-4.2, Paper A-2, p. 20.
238

APPENDIX A
Isotopic Data and Apparent Ages for Various generations of Uraninite from the Beaverlodge area
Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
Cataclasite-type uraninite
6122-Cat_6b Ace Fay 0.125 0.002 4.36 0.47 0.26 0.01 0.22 2023 24 1493 690 1705 90 26
6122-Cat_7b Ace Fay 0.1020 0.0004 2.84 0.18 0.21 0.03 1.00 1660 8 1223 510 1366 46 26
6122-Cat_11c Ace Fay 0.102 0.001 3.47 0.58 0.23 0.04 0.30 1668 20 1338 187 1521 132 20
6122-Cat_14b Ace Fay 0.112 0.003 3.89 0.53 0.25 0.03 0.19 1829 50 1421 161 1612 110 22
6122-Cat_16b Ace Fay 0.1345 0.0003 4.29 0.34 0.25 0.03 0.90 2158 4 1463 419 1691 65 32
6122-Cat_22b Ace Fay 0.1335 0.002 4.12 0.32 0.26 0.04 0.24 2144 25 1491 194 1659 63 30
6122-Cat_24a Ace Fay 0.145 0.001 5.28 0.11 0.31 0.03 1.00 2293 17 1718 298 1866 18 25
6122-Cat_24c Ace Fay 0.117 0.003 4.30 0.11 0.26 0.02 0.86 1903 46 1468 391 1693 216 23
6122-Cat_26b Ace Fay 0.128 0.002 3.42 0.84 0.22 0.03 0.62 2066 29 1305 366 1510 195 37
6122-Cat_28a Ace Fay 0.134 0.003 4.49 0.10 0.27 0.02 0.05 2155 37 1522 364 1729 168 29
6122-Cat_29b Ace Fay 0.132 0.002 3.03 0.45 0.21 0.03 0.78 2126 26 1237 523 1415 115 42
Early tensional vein-type uraninite
6122BV_Cat_9c Ace Fay 0.085 0.002 3.22 0.68 0.24 0.07 0.66 1310 49 1396 373 1461 166 -7
6122BV_Cat_11a Ace Fay 0.094 0.002 3.2 0.6 0.23 0.08 0.63 1505 43 1360 405 1456 144 10
6122BV_Cat_14d Ace Fay 0.089 0.000 4.1 0.5 0.31 0.02 0.22 1399 5 1753 117 1655 101 -25
6122BV_Cat_16d Ace Fay 0.113 0.002 3.37 0.54 0.24 0.05 0.01 1851 28 1399 270 1498 125 24
6122BV_Cat_16f Ace Fay 0.098 0.002 3.2 0.4 0.24 0.05 0.21 1586 44 1409 274 1467 108 11
6122BV_Cat_17b Ace Fay 0.135 0.003 3.7 0.6 0.27 0.05 0.92 2158 39 1525 267 1579 134 29
6122BV_Cat_21c Ace Fay 0.097 0.003 3.3 0.5 0.24 0.08 0.15 1573 67 1364 393 1481 117 13
6122BV_Cat_22c Ace Fay 0.113 0.003 3.54 0.31 0.26 0.04 0.08 1855 55 1510 183 1536 70 19
6122BV_Cat_22d Ace Fay 0.103 0.001 3.1 0.2 0.23 0.04 1.00 1682 11 1328 208 1430 41 21
6122BV_Cat_22e Ace Fay 0.096 0.002 3.79 0.24 0.28 0.07 0.11 1540 35 1582 333 1590 51 -3
6122BV_Cat_25a Ace Fay 0.145 0.002 3.49 0.36 0.25 0.05 0.62 2289 20 1448 234 1525 82 37
6122BV_Cat_25d Ace Fay 0.114 0.003 3.5 0.6 0.26 0.05 0.20 1864 45 1469 232 1536 128 21
6122BV_Cat_27e Ace Fay 0.094 0.001 3.77 0.23 0.29 0.10 0.53 1503 28 1628 483 1587 49 -8
6122BV_Cat_29e Ace Fay 0.103 0.002 4.0 1.0 0.30 0.09 0.70 1682 44 1688 433 1634 198 0
6122a Ace Fay 0.099 0.001 2.25 0.23 0.17 0.02 1.00 1599 12 987 91 1197 71 38
6122b Ace Fay 0.088 0.003 1.40 0.14 0.11 0.01 0.98 1387 58 701 50 889 59 49
239

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
Gunnar type-uraninite
6037b_1 Gunnar 0.0571 0.0007 0.24 0.02 0.030 0.002 0.99 497 26 190 14 215 15 62
6037b_2 Gunnar 0.0530 0.0003 0.28 0.01 0.039 0.001 0.98 329 15 246 8 254 7 25
6037b_3 Gunnar 0.0533 0.0006 0.33 0.02 0.045 0.002 0.98 341 25 283 13 289 12 17
6037b_4 Gunnar 0.055 0.001 0.29 0.02 0.039 0.001 1.00 394 49 246 9 261 13 38
6037b_5 Gunnar 0.0531 0.0006 0.23 0.01 0.031 0.001 0.97 335 28 197 9 208 9 41
6037b_6 Gunnar 0.053 0.001 0.17 0.01 0.024 0.001 0.93 326 42 151 7 161 7 54
6037b_7 Gunnar 0.054 0.002 0.17 0.02 0.022 0.002 0.99 373 93 141 13 156 19 62
6037b_8 Gunnar 0.053 0.003 0.16 0.04 0.022 0.004 1.00 324 138 141 22 153 33 57
6037b_9 Gunnar 0.054 0.001 0.37 0.32 0.050 0.042 1.00 362 62 315 255 323 238 13
6037b_10 Gunnar 0.051 0.003 0.11 0.02 0.016 0.002 0.95 238 130 102 12 109 15 57
6134 Gunnar 0.084 0.005 0.09 0.01 0.0075 0.0004 0.77 1290 126 48 3 85 8 96
6134e Gunnar 0.077 0.003 0.44 0.10 0.0419 0.0098 0.99 1122 87 264 60 373 73 76
6134g Gunnar 0.074 0.003 0.015 0.001 0.00151 0.00002 0.36 1037 87 10 0 15 1 99
6134j Gunnar 0.0866 0.0004 0.33 0.01 0.027 0.001 0.99 1352 9 175 8 288 11 87
6134k Gunnar 0.0867 0.0004 0.29 0.01 0.0242 0.0007 1.00 1353 9 154 5 258 8 89
6134l Gunnar 0.0866 0.0005 0.34 0.04 0.028 0.003 1.00 1351 11 179 21 293 31 87
6134m Gunnar 0.0875 0.0002 0.31 0.01 0.0258 0.0009 0.05 1372 4 164 5 274 8 88
GN-42 Gunnar 0.0787 0.0007 0.34 0.04 0.032 0.004 1.00 1164 18 201 23 300 30 83
GN-42_1 Gunnar 0.0786 0.0012 0.35 0.01 0.032 0.001 0.93 1162 31 204 8 304 11 82
GN-42_2 Gunnar 0.0791 0.0009 0.32 0.02 0.029 0.002 0.99 1174 23 186 14 281 17 84
GN-42_3 Gunnar 0.084 0.001 0.47 0.03 0.041 0.003 0.99 1284 22 256 17 389 21 80
GN-42_4 Gunnar 0.081 0.001 0.38 0.02 0.034 0.002 0.99 1222 25 217 15 329 17 82
GN-42_6 Gunnar 0.0788 0.0009 0.34 0.03 0.031 0.002 0.99 1166 23 196 15 294 19 83
GN-42_8 Gunnar 0.0830 0.0007 0.44 0.04 0.038 0.004 1.00 1270 16 243 22 370 29 81
GN-42_9 Gunnar 0.0807 0.0015 0.37 0.03 0.033 0.002 0.97 1213 38 209 14 317 21 83
GN-42_10 Gunnar 0.0822 0.0008 0.40 0.02 0.035 0.002 0.98 1250 18 223 11 341 15 82
GN-42_11 Gunnar 0.0796 0.0009 0.36 0.02 0.033 0.002 0.99 1187 22 208 14 312 19 82
GN-42_12 Gunnar 0.081 0.002 0.39 0.03 0.035 0.003 0.96 1221 48 224 17 338 24 82
VR69190-2 Gunnar 0.0652 0.0005 0.653 0.049 0.073 0.005 0.99 782 18 452 32 510 30 42
VR69190-3 Gunnar 0.0655 0.0005 0.678 0.042 0.075 0.005 0.99 790 16 467 28 525 26 41
VR69190-4 Gunnar 0.0649 0.0006 0.557 0.042 0.062 0.005 0.99 772 20 389 29 449 28 50
VR69190-5 Gunnar 0.0651 0.0009 0.566 0.049 0.063 0.006 0.99 777 29 395 35 456 32 49
VR69190-7 Gunnar 0.0657 0.0005 0.683 0.043 0.075 0.005 0.99 796 15 469 28 528 26 41
VR69190-8 Gunnar 0.0656 0.0008 0.674 0.046 0.074 0.005 0.99 795 25 463 31 523 28 42
VR69190-9 Gunnar 0.0655 0.0006 0.733 0.050 0.081 0.006 0.99 791 19 503 34 559 29 36
240

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
VR69190-10 Gunnar 0.0653 0.0007 0.599 0.050 0.067 0.006 0.99 783 21 415 34 476 32 47
VR69190-11 Gunnar 0.0652 0.0004 0.596 0.025 0.066 0.003 0.99 782 12 414 17 475 16 47
VR69190-12 Gunnar 0.0654 0.0006 0.613 0.055 0.068 0.006 1.00 788 19 424 35 486 35 46
Breccia type-uraninite
B5812_1 Ace Fay 0.104 0.002 3.12 0.07 0.197 0.026 0.15 1698 39 1157 140 1437 17 32
B5812_2 Ace Fay 0.112 0.003 2.04 0.01 0.126 0.025 0.50 1825 44 767 142 1130 2 58
B5812_3 Ace Fay 0.110 0.002 2.61 0.01 0.153 0.011 0.50 1802 33 920 64 1304 2 49
B5812_4 Ace Fay 0.110 0.004 2.32 0.05 0.146 0.022 0.32 1800 74 879 125 1218 16 51
B5812_5 Ace Fay 0.108 0.004 2.58 0.03 0.160 0.004 0.59 1759 67 958 25 1294 7 46
B5812_6 Ace Fay 0.1130 0.0003 2.72 0.02 0.168 0.010 0.50 1848 5 1001 57 1335 5 46
B5812_7 Ace Fay 0.109 0.002 3.48 0.05 0.219 0.004 0.50 1778 42 1278 23 1523 12 28
B5812_8 Ace Fay 0.111 0.001 2.77 0.07 0.196 0.056 0.29 1812 24 1155 299 1349 20 36
B5812_9 Ace Fay 0.101 0.001 3.52 0.05 0.234 0.058 0.16 1649 24 1353 305 1531 11 18
B5812_10 Ace Fay 0.107 0.005 2.41 0.03 0.166 0.046 0.31 1742 88 990 252 1247 9 43
B5812_11 Ace Fay 0.112 0.003 3.90 0.64 0.255 0.088 0.64 1838 53 1465 451 1613 133 20
B5812_12 Ace Fay 0.066 0.001 1.23 0.11 0.090 0.015 0.50 802 31 557 87 814 50 31
C23-116 Cinch Lake 0.073 0.007 0.22 0.07 0.022 0.008 0.99 1010 188 143 50 201 57 86
C23-116a Cinch Lake 0.078 0.002 0.55 0.05 0.051 0.005 0.97 1145 49 320 33 443 34 72
C23-116b Cinch Lake 0.072 0.001 0.37 0.01 0.038 0.001 0.98 986 16 238 6 322 8 76
C23-116d Cinch Lake 0.072 0.001 0.37 0.01 0.038 0.001 0.99 986 16 238 6 322 8 76
C23-116e Cinch Lake 0.079 0.001 0.74 0.04 0.068 0.005 0.99 1164 24 426 27 563 25 63
C23-116f Cinch Lake 0.075 0.002 0.06 0.02 0.006 0.002 0.50 1069 43 38 11 61 19 96
C23-116n Cinch Lake 0.072 0.001 0.56 0.10 0.057 0.011 1.00 992 37 357 69 455 67 64
C23-116o Cinch Lake 0.076 0.000 0.63 0.15 0.060 0.015 1.00 1089 7 376 90 494 97 65
C23-116p Cinch Lake 0.070 0.003 0.26 0.06 0.027 0.007 0.99 929 83 173 45 235 50 81
C23-116q Cinch Lake 0.073 0.004 0.18 0.08 0.018 0.009 1.00 1016 122 115 55 165 67 89
C23-116r Cinch Lake 0.076 0.000 0.95 0.02 0.091 0.003 0.99 1093 10 563 15 680 13 49
C23-116s Cinch Lake 0.070 0.001 0.46 0.09 0.048 0.009 1.00 916 34 300 55 382 62 67
C23-116t Cinch Lake 0.077 0.001 0.57 0.08 0.054 0.008 1.00 1120 27 340 51 461 55 70
C23-116u Cinch Lake 0.074 0.001 0.37 0.07 0.036 0.007 1.00 1052 23 227 44 318 55 78
C23-116v Cinch Lake 0.077 0.001 0.22 0.04 0.020 0.004 1.00 1127 32 130 27 199 37 88
C23-116w Cinch Lake 0.070 0.002 0.21 0.04 0.022 0.004 0.99 936 66 137 26 192 31 85
C23-116x Cinch Lake 0.066 0.001 0.32 0.05 0.034 0.006 1.00 822 28 218 35 278 40 73
C23-116y Cinch Lake 0.075 0.000 0.61 0.08 0.060 0.008 1.00 1056 13 374 46 486 48 65
C23-116zb Cinch Lake 0.075 0.001 0.39 0.09 0.038 0.009 1.00 1065 29 238 57 333 68 78
241

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
C23-116zc Cinch Lake 0.073 0.001 0.26 0.05 0.026 0.005 1.00 1007 20 163 31 232 41 84
C23-116zd Cinch Lake 0.073 0.001 1.08 0.05 0.107 0.006 0.97 1016 34 657 35 744 23 35
C23-116ze Cinch Lake 0.068 0.003 0.35 0.03 0.037 0.002 0.85 854 105 236 15 303 25 72
C23-116zf Cinch Lake 0.071 0.001 0.19 0.03 0.019 0.003 1.00 954 29 124 18 176 22 87
C23-116zg Cinch Lake 0.074 0.001 0.46 0.06 0.045 0.007 1.00 1039 15 286 41 386 45 72
VRC2 Gunnar 0.0840 0.0003 1.60 0.09 0.138 0.008 1.00 1293 6 836 45 972 35 35
VRC3 Gunnar 0.0838 0.0004 1.58 0.05 0.137 0.004 0.99 1288 10 826 21 962 18 36
VRC4 Gunnar 0.0879 0.0015 1.09 0.03 0.090 0.001 1.00 1380 34 553 5 747 14 60
VRC5 Gunnar 0.0855 0.0002 1.74 0.07 0.147 0.006 1.00 1327 4 887 32 1023 25 33
VRC7 Gunnar 0.0850 0.0002 1.50 0.06 0.128 0.006 1.00 1316 5 778 32 932 26 41
VRC8 Gunnar 0.0851 0.0003 1.31 0.07 0.112 0.006 1.00 1318 7 683 33 851 29 48
VRC9 Gunnar 0.0848 0.0002 1.42 0.08 0.121 0.007 1.00 1312 4 738 42 897 35 44
VRC10 Gunnar 0.0860 0.0002 1.71 0.05 0.144 0.004 1.00 1338 4 869 23 1012 18 35
VRC11 Gunnar 0.0865 0.0003 1.77 0.07 0.148 0.006 0.99 1349 8 891 31 1033 25 34
VRC12 Gunnar 0.0857 0.0006 1.30 0.07 0.110 0.006 0.99 1332 14 673 34 846 30 49
VRC13 Gunnar 0.0854 0.0004 1.47 0.09 0.125 0.008 1.00 1325 9 757 44 916 36 43
VRC14 Gunnar 0.0864 0.0002 2.08 0.07 0.174 0.006 1.00 1348 5 1036 33 1142 23 23
VRC15 Gunnar 0.0867 0.0002 2.04 0.07 0.171 0.006 1.00 1354 5 1017 30 1130 22 25
VRC16 Gunnar 0.087 0.001 2.13 0.09 0.178 0.008 0.96 1356 24 1054 42 1157 31 22
Volcanic type-uraninite
6120a Ace Fay 0.1073 0.0002 2.98 0.12 0.202 0.008 1.00 1754 4 1184 44 1403 30 32
6120b Ace Fay 0.1085 0.0002 3.43 0.19 0.229 0.012 0.89 1774 4 1331 61 1511 43 25
6120c Ace Fay 0.1078 0.0005 4.45 0.31 0.299 0.020 1.00 1763 9 1688 101 1722 58 4
6120e Ace Fay 0.1081 0.0003 3.41 0.09 0.229 0.006 1.00 1768 5 1329 33 1507 21 25
6120f Ace Fay 0.1072 0.0005 3.70 0.19 0.250 0.012 1.00 1753 8 1441 63 1572 42 18
6120g Ace Fay 0.1065 0.0001 3.36 0.11 0.229 0.007 1.00 1740 2 1328 38 1495 25 24
6120i Ace Fay 0.1080 0.0004 3.51 0.10 0.235 0.007 0.99 1766 6 1363 36 1529 24 23
6120k Ace Fay 0.1075 0.0005 3.27 0.13 0.221 0.009 0.99 1758 9 1285 48 1474 30 27
6120l Ace Fay 0.1067 0.0003 3.43 0.29 0.233 0.019 1.00 1743 5 1352 101 1512 67 22
6120m Ace Fay 0.1085 0.0003 3.69 0.25 0.246 0.017 1.00 1775 4 1420 85 1569 55 20
6120n Ace Fay 0.1054 0.0005 2.83 0.17 0.195 0.012 1.00 1722 9 1146 66 1363 45 33
6120q Ace Fay 0.1100 0.0023 2.99 0.34 0.208 0.033 0.52 1800 37 1218 178 1405 86 32
6139a Gunnar 0.1097 0.0001 4.74 0.28 0.316 0.019 1.00 1794 2 1768 91 1774 49 1
6139b Gunnar 0.1096 0.0001 4.53 0.20 0.302 0.014 1.00 1792 2 1702 69 1737 38 5
6139d Gunnar 0.1094 0.0002 4.55 0.29 0.304 0.019 1.00 1789 4 1711 94 1740 53 4
242

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
6139e Gunnar 0.1085 0.0004 4.0 0.4 0.271 0.028 1.00 1775 7 1545 140 1639 84 13
6139f Gunnar 0.1094 0.0001 4.40 0.32 0.294 0.021 1.00 1789 2 1662 106 1713 60 7
6139g Gunnar 0.1100 0.0001 4.52 0.23 0.300 0.015 1.00 1799 2 1692 77 1734 43 6
6139h Gunnar 0.1095 0.0002 4.2 0.4 0.281 0.024 1.00 1791 3 1595 121 1676 70 11
6139i Gunnar 0.1094 0.0003 4.30 0.22 0.287 0.016 1.00 1790 5 1627 79 1693 43 9
6139j Gunnar 0.1102 0.0001 4.56 0.26 0.302 0.017 1.00 1803 1 1703 85 1742 47 6
6139k Gunnar 0.1091 0.0002 4.52 0.17 0.303 0.011 1.00 1784 3 1707 56 1735 31 4
6139l Gunnar 0.1093 0.0002 4.51 0.32 0.301 0.021 1.00 1787 3 1698 106 1732 60 5
6139m Gunnar 0.1101 0.0001 3.96 0.28 0.264 0.019 1.00 1800 2 1508 94 1626 57 16
6139n Gunnar 0.1104 0.0003 4.0 0.4 0.268 0.025 1.00 1806 5 1529 127 1641 74 15
6139o Gunnar 0.1101 0.0002 4.0 0.4 0.268 0.024 1.00 1801 4 1529 121 1639 71 15
6139p Gunnar 0.1098 0.0002 3.71 0.29 0.247 0.019 1.00 1797 4 1422 101 1573 62 21
6139q Gunnar 0.1098 0.0003 3.66 0.29 0.244 0.020 1.00 1795 4 1406 102 1562 64 22
6139r Gunnar 0.1108 0.0009 4.0 0.3 0.268 0.019 0.99 1812 15 1529 94 1641 53 16
6139s Gunnar 0.1080 0.0005 3.3 0.5 0.226 0.033 1.00 1766 8 1315 171 1490 111 26
6139t Gunnar 0.1106 0.0002 4.21 0.38 0.279 0.025 1.00 1809 4 1584 125 1677 73 12
6139u Gunnar 0.1099 0.0002 4.14 0.42 0.276 0.028 1.00 1797 4 1569 143 1662 83 13
6139v Gunnar 0.1084 0.0005 3.56 0.33 0.241 0.023 1.00 1773 8 1390 117 1541 74 22
6139vna Gunnar 0.1097 0.0001 4.63 0.24 0.309 0.016 1.00 1794 2 1734 79 1755 44 3
EA3011 Eagle-Ace 0.0524 0.0008 0.25 0.01 0.035 0.002 0.96 303 36 222 13 229 12 27
EA3011a Eagle-Ace 0.0523 0.0006 0.23 0.03 0.032 0.004 0.99 300 28 202 25 210 24 33
EA3011b Eagle-Ace 0.0536 0.0003 0.26 0.01 0.035 0.002 1.00 354 11 221 11 232 10 38
EA3011c Eagle-Ace 0.0537 0.0008 0.23 0.02 0.031 0.003 0.99 360 35 198 18 211 20 45
EA3011d Eagle-Ace 0.0519 0.0010 0.21 0.02 0.029 0.002 0.97 282 43 186 13 193 14 34
EA3011e Eagle-Ace 0.0531 0.0004 0.27 0.01 0.037 0.002 0.99 334 17 232 10 241 10 31
EA3011f Eagle-Ace 0.0535 0.0003 0.26 0.02 0.036 0.002 1.00 348 14 225 15 236 14 35
EA3011g Eagle-Ace 0.0516 0.0009 0.18 0.01 0.025 0.001 0.97 269 40 158 9 166 10 41
EA3011h Eagle-Ace 0.0514 0.0013 0.21 0.02 0.030 0.003 0.98 259 59 188 20 193 21 27
EA3011j Eagle-Ace 0.0525 0.0007 0.20 0.02 0.027 0.002 0.99 306 31 172 15 181 14 44
EA3011k Eagle-Ace 0.0539 0.0005 0.29 0.02 0.039 0.003 0.99 369 20 247 17 259 16 33
EA3011l Eagle-Ace 0.0540 0.0002 0.30 0.01 0.040 0.001 0.99 373 10 254 8 266 8 32
EA3011n Eagle-Ace 0.0529 0.0006 0.20 0.02 0.028 0.002 0.99 323 26 176 13 186 13 46
EA3011o Eagle-Ace 0.0518 0.0005 0.19 0.02 0.027 0.003 1.00 278 24 173 18 180 17 38
EA3011t Eagle-Ace 0.0552 0.0005 0.31 0.01 0.040 0.001 0.96 419 21 254 7 271 8 39
Athabasca type-uraninite
243

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
2202p2 Martin Lake 0.0896 0.0003 2.33 0.16 0.190 0.013 1.00 1416 7 1123 68 1223 48 21
2202p2-1 Martin Lake 0.0859 0.0004 1.80 0.10 0.153 0.009 1.00 1336 8 920 50 1047 36 31
2202p2-2 Martin Lake 0.0890 0.0008 2.20 0.14 0.180 0.013 1.00 1404 16 1069 70 1180 45 24
2202p2-3 Martin Lake 0.0863 0.0002 2.0 0.2 0.171 0.013 1.00 1345 4 1018 73 1122 52 24
2202p2-4 Martin Lake 0.0931 0.0002 2.05 0.08 0.161 0.006 1.00 1489 4 963 36 1133 28 35
2202p2-5 Martin Lake 0.0841 0.0002 1.82 0.16 0.159 0.014 1.00 1295 4 949 77 1054 58 27
2202p2-6 Martin Lake 0.0882 0.0003 2.09 0.06 0.173 0.005 0.99 1388 6 1029 27 1145 19 26
2202p2-7 Martin Lake 0.0922 0.0003 2.21 0.13 0.175 0.010 1.00 1471 5 1039 58 1183 42 29
2202p2-8 Martin Lake 0.0891 0.0004 1.86 0.11 0.153 0.010 1.00 1407 8 915 54 1067 40 35
2202p2-9 Martin Lake 0.0901 0.0002 2.34 0.15 0.190 0.012 1.00 1427 4 1119 67 1223 46 22
2202p2-11 Martin Lake 0.0901 0.0004 2.26 0.15 0.183 0.012 1.00 1429 9 1083 67 1198 45 24
2202p2-12 Martin Lake 0.0906 0.0006 2.1 0.2 0.167 0.012 1.00 1439 13 997 66 1141 53 31
2202p2-13 Martin Lake 0.0890 0.0001 2.0 0.1 0.168 0.012 1.00 1404 3 999 64 1129 47 29
2202p2-14 Martin Lake 0.0866 0.0004 2.0 0.1 0.170 0.011 1.00 1351 9 1012 61 1120 44 25
2202p2-15 Martin Lake 0.0890 0.0007 2.21 0.16 0.181 0.012 1.00 1404 14 1075 65 1184 50 23
2202p2-16 Martin Lake 0.0857 0.0005 2.0 0.2 0.170 0.016 1.00 1332 10 1012 88 1114 67 24
2202p2-17 Martin Lake 0.0873 0.0005 2.1 0.1 0.178 0.013 1.00 1367 11 1054 69 1156 48 23
2202p2-18 Martin Lake 0.0914 0.0006 2.43 0.19 0.194 0.015 1.00 1456 13 1144 81 1252 57 21
2202p2-19 Martin Lake 0.0901 0.0002 2.25 0.11 0.182 0.009 1.00 1427 5 1080 51 1196 35 24
2202p2-21 Martin Lake 0.0998 0.0002 3.1 0.2 0.229 0.017 1.00 1620 4 1327 91 1438 58 18
2202p2-22 Martin Lake 0.0850 0.0003 1.74 0.11 0.149 0.010 1.00 1316 6 898 54 1023 40 32
2202p2-23 Martin Lake 0.0983 0.0003 2.99 0.22 0.222 0.016 1.00 1593 5 1295 85 1406 56 19
2202p2-24 Martin Lake 0.0855 0.0005 1.98 0.17 0.169 0.014 1.00 1326 12 1006 75 1108 58 24
2202p2-25 Martin Lake 0.0993 0.0006 3.0 0.2 0.224 0.013 1.00 1611 12 1302 69 1419 43 19
2202p2-26 Martin Lake 0.0894 0.0001 2.0 0.1 0.167 0.012 1.00 1413 2 993 64 1128 48 30
2202p2-27 Martin Lake 0.0952 0.0012 2.35 0.11 0.180 0.010 0.98 1532 24 1068 56 1226 34 30
2202p2-28 Martin Lake 0.0969 0.0008 2.85 0.10 0.215 0.008 0.98 1565 15 1255 44 1368 26 20
2202p2-29 Martin Lake 0.0934 0.0023 2.64 0.36 0.206 0.023 1.00 1496 47 1208 123 1312 100 19
2202p2-31 Martin Lake 0.0875 0.0005 1.76 0.12 0.147 0.010 1.00 1371 11 882 55 1030 45 36
2202p2-32 Martin Lake 0.0872 0.0001 1.59 0.08 0.134 0.006 1.00 1364 2 808 37 968 30 41
2202p2-33 Martin Lake 0.0870 0.0003 2.0 0.1 0.170 0.010 1.00 1361 6 1013 53 1124 39 26
2202p1 Martin Lake 0.0880 0.0004 2.1 0.2 0.171 0.014 1.00 1383 8 1019 75 1136 52 26
2202p1-2 Martin Lake 0.0881 0.0002 1.69 0.06 0.140 0.005 1.00 1384 5 845 29 1004 24 39
2202p1-33 Martin Lake 0.0906 0.0002 1.88 0.08 0.151 0.006 1.00 1438 5 908 36 1073 27 37
2202p1-34 Martin Lake 0.0851 0.0002 1.48 0.09 0.127 0.008 1.00 1317 5 772 45 923 38 41
2202p1-35 Martin Lake 0.0884 0.0005 1.52 0.06 0.126 0.006 1.00 1392 10 764 33 940 25 45
244

Sample
Deposit
207 Pb/ 206 Pb ±2σ
207 Pb/ 235 U ±2σ
206 Pb/ 238 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
2202p1-36 Martin Lake 0.0880 0.0002 1.56 0.08 0.130 0.006 1.00 1382 5 785 37 954 32 43
EA3010A Eagle-Ace 0.0540 0.0003 0.29 0.01 0.039 0.002 1.00 373 11 248 12 261 11 33
EA3010A-1 Eagle-Ace 0.0539 0.0003 0.27 0.02 0.036 0.003 1.00 366 12 229 16 241 15 38
EA3010A-2 Eagle-Ace 0.0539 0.0002 0.28 0.03 0.037 0.004 1.00 367 9 235 24 247 23 36
EA3010A-3 Eagle-Ace 0.0531 0.0004 0.26 0.02 0.036 0.002 0.99 333 16 228 14 237 14 32
EA3010A-4 Eagle-Ace 0.0543 0.0004 0.27 0.02 0.036 0.003 1.00 385 19 229 16 243 14 41
EA3010A-5 Eagle-Ace 0.0524 0.0004 0.24 0.02 0.034 0.003 1.00 302 16 213 16 220 16 30
EA3010A-6 Eagle-Ace 0.0537 0.0004 0.26 0.03 0.035 0.004 1.00 360 17 224 25 236 24 38
EA3010A-7 Eagle-Ace 0.0516 0.0003 0.21 0.02 0.029 0.003 1.00 269 15 185 20 192 19 31
EA3010A-8 Eagle-Ace 0.0528 0.0004 0.25 0.01 0.034 0.002 0.99 320 16 216 13 225 12 32
EA3010A-9 Eagle-Ace 0.0546 0.0003 0.30 0.02 0.039 0.002 0.99 396 13 248 12 262 12 38
245

APPENDIX B
REE contents of various generation of uraninite from the deposits of the Beaverlodge area
Sample Y Zr Cs Ba Th La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
6120-1 395.4 1124.4 0.3 1615.1 84.27 1502.3 2267.9 181.4 471.9 42.4 10.5 44.8 5.8 39.3 8.4 25.0 3.4 22.2 3.1
6120-3 519.2 1150.5 0.3 848.9 40.99 1127.4 1478.6 112.0 310.7 34.2 8.6 46.6 6.2 43.0 9.7 27.9 3.7 24.3 3.7
6120-4 394.4 1268.9 0.3 1068.9 69.55 1414.3 2016.8 154.9 391.0 33.9 7.9 35.9 4.8 33.3 7.1 20.7 2.8 18.6 2.8
6120-5 452.7 1113.7 0.2 1208.2 63.73 1553.0 2260.4 186.0 519.3 51.4 11.9 52.9 7.5 50.2 10.5 29.2 3.9 24.5 3.4
6120-8 552.4 1210.1 0.3 927.8 69.96 1713.6 2312.2 188.7 550.8 62.5 14.6 69.8 9.9 65.0 13.6 39.2 5.0 29.8 4.4
6120-10 411.8 1085.0 0.3 892.3 56.26 1287.5 1866.2 151.3 393.7 37.6 9.5 41.6 5.6 38.8 8.1 23.2 3.1 20.6 3.0
6120-11 469.4 1329.7 0.2 773.4 74.18 1833.3 2728.2 230.0 632.1 57.7 14.0 54.5 7.0 46.4 9.9 27.5 3.8 24.6 3.4
3705-1 910.0 2002.0 9.1 1210.8 607.24 1459.7 4766.3 390.1 1181.7 248.0 41.6 152.1 29.1 198.6 35.6 92.2 15.3 87.6 10.9
3705-2 634.6 1825.4 2.2 850.7 590.77 1175.1 4674.0 468.8 1617.6 288.7 49.1 172.4 31.2 197.3 35.5 100.5 14.9 91.1 10.9
3705-3 765.9 1486.8 6.8 875.0 492.21 1775.0 6435.4 573.9 1869.6 312.8 53.4 214.5 36.0 233.2 41.4 121.2 16.3 110.0 14.4
3705-4 989.8 2018.2 2.3 774.7 521.64 1948.2 6666.6 601.0 2047.4 347.8 58.3 220.0 38.2 244.7 43.8 125.7 18.4 117.8 14.4
3705-5 318.6 1770.7 0.5 1031.2 650.85 893.9 2913.2 237.8 844.7 115.8 20.4 69.4 12.3 74.0 13.7 35.1 5.1 34.0 3.8
3705-6 532.9 1821.9 1.8 776.4 382.13 1157.4 4863.5 442.2 1411.6 215.9 38.3 140.8 26.9 182.0 30.1 93.9 14.2 101.3 11.6
3705-7 187.9 2732.4 1.8 1322.6 687.03 718.4 2384.4 208.9 670.4 93.3 16.9 52.4 9.8 64.3 10.4 27.6 4.3 26.7 3.6
3705-8 130.5 4649.5 1.9 1276.3 1110.85 544.1 1627.9 138.4 432.0 60.9 9.9 36.5 6.0 42.0 6.7 18.8 2.8 19.2 2.2
3705-10 148.5 8107.2 8.0 1621.4 1075.82 399.4 1224.4 105.2 360.6 58.6 7.7 39.4 6.7 44.4 7.6 23.5 4.1 27.2 3.0
3705-12 465.0 2257.5 1.2 948.8 827.95 1571.3 5964.9 511.0 1625.1 258.8 41.3 145.7 26.8 178.6 29.6 80.7 12.6 86.7 9.8
5812_1 5517.2 7031.7 0.1 69.8 803.7 1473.1 2587.5 345.7 1608.8 458.2 112.6 718.3 119.4 854.0 177.8 485.6 61.6 344.7 42.4
5812_2 5467.8 7113.0 0.6 422.6 2202.3 2010.3 4375.0 616.7 2937.2 790.8 173.4 778.6 141.6 943.7 187.5 527.6 68.6 426.6 52.6
5812_3 3309.7 8056.2 6.8 3289.2 7150.2 4789.0 7968.2 903.1 3369.1 866.5 174.9 732.5 138.8 972.8 187.4 540.7 72.6 419.7 49.9
5812_5 2218.5 10919.2 0.3 2684.7 3117.8 1769.4 6915.6 919.6 3302.0 614.1 121.5 394.1 79.4 559.1 103.9 302.8 48.7 339.1 39.2
5812_8 3190.0 9671.6 1.1 1690.4 2584.7 3536.8 7751.8 886.5 3322.5 683.1 160.7 566.2 104.4 714.0 129.0 368.3 56.0 370.9 43.5
5812_9 8937.3 299758.8 7.2 2289.5 7459.0 3508.8 8452.6 1036.5 4487.9 1258.8 192.6 1199.0 263.1 2017.8 401.3 1249.2 246.5 1867.3 221.7
5812_10 296.5 8372.7 0.7 2840.3 4543.5 1444.3 2214.2 174.0 487.0 85.1 16.5 61.1 12.0 86.5 14.8 39.8 6.8 43.3 5.2
5812_11 1150.9 5126.7 0.1 289.3 2668.1 1585.3 2494.8 275.8 990.1 190.2 44.3 184.0 31.6 223.4 43.5 115.2 16.3 105.3 12.1
90085-1 3006.9 2913.6 0.4 150.0 1441.4 1676.0 3607.3 476.3 2106.9 532.0 128.2 522.9 85.5 571.7 108.0 293.9 38.6 234.6 28.3
90085-2 4783.0 3209.7 0.2 87.3 1901.3 2015.6 3993.8 542.6 2464.9 673.4 168.2 676.0 116.1 800.5 145.7 383.5 54.1 337.1 38.6
90085-3 2407.3 4846.2 0.3 72.8 1420.0 1459.5 2831.5 356.2 1551.3 379.5 99.0 420.8 65.1 463.0 86.8 214.3 29.0 180.1 19.4
246

Sample Y Zr Cs Ba Th La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
90085-4 2997.8 3900.8 0.3 69.1 1542.2 1678.9 3252.0 426.7 1843.8 506.2 120.4 501.3 79.0 508.7 100.7 256.3 34.4 213.3 24.3
90085-5 4270.4 3266.4 0.2 66.3 1912.2 2220.0 4653.4 599.9 2661.6 720.6 166.4 702.8 119.5 793.6 148.0 386.3 53.4 344.4 38.5
90085-6 2182.5 4199.7 0.2 78.6 1013.4 1251.7 2196.5 264.8 1147.7 304.8 74.7 321.1 55.2 384.5 73.9 199.9 27.0 169.7 19.7
90085-7 5088.6 4145.2 0.3 174.1 1538.2 1888.5 3574.8 458.6 2139.1 593.9 158.7 691.8 115.8 791.9 157.3 420.7 56.1 358.1 41.2
90085-8 2111.3 4817.6 0.4 79.8 1218.5 1397.3 2540.5 309.9 1326.8 345.9 81.6 339.6 56.9 383.6 72.8 190.8 26.8 165.1 18.0
90085-9 1838.6 4395.7 0.2 63.2 991.0 1158.3 2097.4 256.2 1158.1 296.7 69.4 296.7 47.6 334.4 60.8 163.4 22.8 142.9 15.5
90085-10 4913.5 2419.0 0.3 138.1 1418.1 1731.2 3981.7 514.2 2460.9 649.1 176.7 734.0 120.1 817.5 155.1 420.8 55.4 339.7 42.1
90085-11 6560.4 2597.1 0.7 400.7 1009.7 2310.0 4095.9 550.8 2804.5 831.6 196.1 948.6 180.0 1319.4 257.1 726.6 104.3 669.1 81.6
6134-12 2049.0 11910.2 0.1 11671.1 87.0 3729.8 1650.0 1505.6 7426.5 1744.4 66.4 1281.9 156.4 875.6 162.7 408.2 57.3 374.7 42.9
6134-10 2661.0 390.6 0.1 9416.2 12.7 3526.3 1739.6 1491.9 7088.4 1601.7 62.4 1204.1 150.2 867.6 158.7 406.4 57.5 383.7 47.0
6134-9 3430.1 186.1 0.1 10570.5 13.4 3031.1 1371.2 1162.3 5581.2 1342.3 52.1 973.2 123.3 728.4 131.3 339.9 48.7 312.2 37.6
6134-8 829.5 1528.5 0.0 11317.2 73.1 2274.2 631.8 440.1 2224.2 578.3 25.6 564.9 69.1 400.7 74.3 190.3 28.9 193.3 22.7
6134-11 3266.0 14.6 0.1 9888.2 1.7 1549.9 244.1 138.5 706.5 174.6 7.9 196.2 22.2 132.6 26.7 71.5 9.9 62.4 8.1
6134-13 208.6 47.2 0.5 9233.4 0.2 795.5 113.9 44.4 222.2 33.7 1.4 34.2 3.4 17.7 4.2 10.4 1.4 7.8 1.1
6134-14 179.8 84.4 0.7 10900.2 0.1 674.2 116.6 43.6 200.7 32.5 1.5 33.1 3.8 20.7 4.5 12.3 1.8 11.7 1.4
6122-22 164.1 1208.6 5.6 5213.4 5.8 822.9 1028.4 119.2 605.6 77.9 15.6 87.3 11.0 73.1 14.7 40.1 5.3 28.3 5.4
6122-21 276.2 2150.6 8.4 14778.3 6.3 680.9 867.5 95.9 391.4 66.9 13.6 67.4 7.7 59.9 10.5 32.3 3.8 27.8 3.7
6122-19 157.9 1104.7 1.9 3467.8 2.9 675.6 863.8 95.6 408.3 65.3 11.9 57.4 7.9 52.1 12.7 34.8 5.4 31.9 4.1
6122-17 265.0 2177.3 1.4 8225.1 6.8 630.9 835.5 92.8 382.0 64.0 13.3 64.0 8.7 58.9 11.8 32.8 4.3 27.5 3.6
6122-18 234.0 1680.8 4.4 3870.5 2.7 640.2 736.2 87.0 342.2 66.9 11.5 64.0 8.9 60.4 12.8 36.9 5.0 30.7 4.5
6122-20 160.6 1482.7 2.0 4759.1 2.7 616.9 682.8 75.0 312.6 57.4 15.8 50.1 7.8 53.4 10.0 32.4 5.0 21.7 3.8
6122-3 178.3 1681.1 1.9 7814.0 2.7 366.9 481.2 39.2 132.8 21.6 4.7 21.7 2.9 20.0 4.4 15.4 2.3 14.8 2.2
6122-11 180.9 1508.2 1.2 7845.6 15.0 317.8 454.6 39.3 133.0 20.3 4.5 17.4 2.3 15.3 3.3 9.5 1.5 9.3 1.7
6122-12 183.7 2199.3 3.0 5415.1 3.6 302.3 376.5 40.4 123.6 14.1 2.4 17.5 2.2 17.8 3.8 12.1 1.9 11.4 2.0
6122-9 267.3 3662.7 2.8 8829.1 6.7 274.8 381.0 35.1 118.2 17.9 4.1 16.6 2.4 16.1 3.3 9.9 1.5 9.9 1.5
6122-2 208.7 1938.7 3.7 5962.3 4.1 231.0 358.1 33.0 120.8 21.0 4.8 23.0 3.4 23.0 4.3 11.7 1.7 14.4 2.0
6122-13 207.8 1844.4 2.3 5888.9 5.1 263.2 342.9 33.7 105.6 17.5 3.6 14.9 2.4 19.1 4.0 11.0 2.0 12.2 1.6
6122-4 473.7 2235.8 0.6 1371.1 86.5 225.8 325.5 30.4 103.1 16.5 4.4 21.6 3.1 23.5 5.4 14.2 2.4 15.6 2.0
6122-5 530.7 2350.1 1.2 4080.8 73.0 285.9 300.8 30.5 89.9 15.0 3.5 19.9 2.3 12.7 4.0 11.3 1.7 12.6 2.1
6122-15 487.5 2227.1 1.6 6451.9 99.1 238.8 292.3 28.5 99.7 17.0 3.4 16.1 2.2 15.5 3.5 10.3 1.5 9.6 1.6
6122-8 443.3 3328.4 3.7 3264.3 78.4 213.5 290.2 29.0 98.0 14.7 3.2 13.4 1.9 14.0 3.1 9.4 1.5 9.8 1.5
6122-6 454.3 2285.9 1.7 3551.7 79.3 214.1 273.0 25.9 77.7 11.7 3.0 16.5 2.1 10.8 2.6 8.6 1.3 6.7 1.2
6122-7 619.7 2209.9 0.7 2175.5 120.8 148.4 224.3 21.0 72.8 10.7 2.2 9.6 1.4 10.1 2.5 7.3 1.2 7.5 1.2
247

Sample Y Zr Cs Ba Th La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu
6139-2 810.9 2096.5 0.3 1048.4 64.2 1384.1 1280.7 126.5 498.2 89.2 19.4 97.0 14.3 99.2 19.9 53.5 7.2 44.6 5.7
6139-3 809.1 1613.8 0.2 510.0 24.6 1533.8 1271.3 122.0 460.2 82.7 18.3 94.7 14.4 101.7 20.7 55.4 7.9 49.4 6.0
6139-4 639.2 1560.8 0.3 1377.8 36.9 1796.1 1485.6 129.3 469.2 72.8 16.6 78.9 12.0 84.2 17.3 46.2 6.5 43.9 4.8
6139-5 749.0 1829.4 0.4 1815.1 45.8 1032.3 1127.3 115.5 480.0 89.9 19.1 91.8 13.9 92.5 19.5 49.8 6.9 43.4 5.3
6139-6 856.0 1404.6 0.5 6402.1 46.9 1571.9 1978.3 172.3 586.1 99.7 24.3 106.2 17.7 129.8 25.9 69.5 9.9 61.0 8.1
6139-7 854.4 2438.0 0.4 2212.6 17.5 1100.9 1179.8 112.0 472.2 88.7 20.6 104.2 14.4 96.6 19.3 49.9 6.4 39.8 5.2
6139-8 776.6 1722.9 2.0 803.4 11.3 922.8 916.7 94.1 388.5 73.9 16.9 84.0 12.7 87.8 18.6 50.7 6.7 42.1 5.6
6139-9 921.3 1978.3 0.8 1015.4 42.7 1197.1 1228.3 127.1 521.8 100.5 22.7 118.0 16.6 113.1 22.4 59.4 7.7 49.8 6.3
6139-11 853.4 35639.6 0.5 7346.8 19.5 583.2 614.8 59.0 241.7 51.7 13.7 71.1 11.5 82.9 18.8 54.6 8.6 58.0 8.1
248

APPENDIX C
REE characteristic parameters of various generation of uraninite from deposits of the
Beaverlodge area.
Sample ΣREE TLREE THREE LREE/HREE Eu/Eu* (La/Sm)N (Tb/La)N (Tb/La)N Tb/Yb Sm/La (La/Yb)N
6120-1 4628.5 4476.5 152.0 29.4 0.7 19.4 0.01 0.00 1.1 0.03 41.0
6120-3 3236.6 3071.5 165.1 18.6 0.7 18.1 0.02 0.01 1.1 0.03 28.1
6120-4 4144.8 4018.9 126.0 31.9 0.7 22.9 0.01 0.00 1.1 0.02 46.1
6120-5 4764.1 4582.0 182.1 25.2 0.7 16.6 0.02 0.00 1.3 0.03 38.4
6120-8 5079.1 4842.3 236.9 20.4 0.7 15.0 0.02 0.01 1.4 0.04 34.8
6120-10 3889.7 3745.7 144.0 26.0 0.7 18.8 0.02 0.00 1.1 0.03 37.9
6120-11 5672.4 5495.2 177.2 31.0 0.8 17.4 0.01 0.00 1.2 0.03 45.1
3705-1 8708.6 8087.3 621.3 13.0 0.6 3.2 0.06 0.02 1.4 0.17 10.1
3705-2 8927.3 8273.3 654.0 12.7 0.6 2.2 0.08 0.03 1.5 0.25 7.8
3705-3 11807.0 11020.1 786.9 14.0 0.6 3.1 0.06 0.02 1.4 0.18 9.8
3705-4 12492.5 11669.4 823.1 14.2 0.6 3.1 0.06 0.02 1.4 0.18 10.0
3705-5 5273.3 5025.8 247.5 20.3 0.6 4.2 0.04 0.01 1.5 0.13 15.9
3705-6 8729.9 8129.0 600.9 13.5 0.6 2.9 0.09 0.02 1.1 0.19 6.9
3705-7 4291.4 4092.2 199.1 20.6 0.7 4.2 0.04 0.01 1.6 0.13 16.3
3705-8 2947.5 2813.2 134.2 21.0 0.6 4.9 0.04 0.01 1.3 0.11 17.1
3705-10 2311.8 2155.8 156.0 13.8 0.5 3.7 0.07 0.02 1.1 0.15 8.9
3705-12 10542.9 9972.3 570.6 17.5 0.6 3.3 0.06 0.02 1.3 0.16 11.0
5812_1 9389.7 6585.9 2803.8 2.3 0.6 1.8 0.23 0.08 1.5 0.31 2.6
5812_2 14030.2 10903.4 3126.9 3.5 0.7 1.4 0.21 0.07 1.4 0.39 2.9
5812_3 21185.2 18070.8 3114.4 5.8 0.7 3.0 0.09 0.03 1.4 0.18 6.9
5812_5 15508.5 13642.2 1866.3 7.3 0.7 1.6 0.19 0.04 1.0 0.35 3.2
5812_8 18693.8 16341.5 2352.3 6.9 0.8 2.8 0.10 0.03 1.2 0.19 5.8
5812_9 26403.2 18937.3 7465.8 2.5 0.5 1.5 0.53 0.07 0.6 0.36 1.1
5812_10 4690.6 4421.1 269.5 16.4 0.7 9.3 0.03 0.01 1.2 0.06 20.2
5812_11 6312.0 5580.6 731.4 7.6 0.7 4.6 0.07 0.02 1.3 0.12 9.1
90085-1 11334.7 8526.6 1883.5 4.5 0.7 1.6 0.14 0.05 1.6 0.32 4.3
90085-2 14232.9 9858.4 2551.7 3.9 0.7 1.6 0.17 0.06 1.5 0.33 3.6
90085-3 9697.7 6677.1 1478.5 4.5 0.7 1.9 0.12 0.04 1.5 0.26 4.9
90085-4 10126.3 7828.1 1718.0 4.6 0.7 1.8 0.13 0.05 1.6 0.30 4.8
90085-5 15865.5 11021.9 2586.6 4.3 0.7 1.6 0.16 0.05 1.5 0.32 3.9
90085-6 7659.2 5240.2 1251.0 4.2 0.7 2.2 0.14 0.04 1.4 0.24 4.5
90085-7 13572.8 8813.7 2632.8 3.3 0.8 1.8 0.19 0.06 1.4 0.31 3.2
90085-8 7914.4 6002.1 1253.8 4.8 0.7 2.1 0.12 0.04 1.5 0.25 5.1
90085-9 6868.9 5036.0 1084.0 4.6 0.7 2.2 0.12 0.04 1.4 0.26 4.9
249

Sample ΣREE TLREE THREE LREE/HREE Eu/Eu* (La/Sm)N (Tb/La)N (Tb/La)N Tb/Yb Sm/La (La/Yb)N
90085-10 14839.2 9513.8 2684.8 3.5 0.8 1.4 0.20 0.07 1.5 0.37 3.1
90085-11 14381.9 10788.9 4286.8 2.5 0.7 1.6 0.29 0.08 1.1 0.36 2.1
6134-12 19482.4 16122.7 3359.8 4.8 0.1 1.2 0.10 0.04 1.8 0.47 6.0
6134-10 18785.4 15510.3 3275.1 4.7 0.1 1.2 0.11 0.04 1.7 0.45 5.6
6134-9 15234.8 12540.1 2694.6 4.7 0.1 1.2 0.10 0.04 1.7 0.44 5.9
6134-8 7718.3 6174.2 1544.0 4.0 0.1 2.2 0.08 0.03 1.5 0.25 7.1
6134-11 3350.9 2821.4 529.5 5.3 0.1 4.9 0.04 0.01 1.5 0.11 15.1
6134-13 1291.3 1211.1 80.2 15.1 0.1 13.0 0.01 0.00 1.9 0.04 61.7
6134-14 1158.3 1069.1 89.3 12.0 0.1 11.4 0.02 0.01 1.4 0.05 34.9
6122-22 2934.6 2669.5 265.1 10.1 0.6 5.8 0.03 0.01 1.7 0.09 17.6
6122-21 2329.3 2116.4 212.9 9.9 0.6 5.6 0.04 0.01 1.2 0.10 14.9
6122-19 2326.9 2120.5 206.4 10.3 0.6 5.7 0.05 0.01 1.1 0.10 12.8
6122-17 2230.0 2018.5 211.5 9.5 0.6 5.4 0.04 0.01 1.3 0.10 13.9
6122-18 2107.2 1884.0 223.2 8.4 0.5 5.2 0.05 0.01 1.2 0.10 12.6
6122-20 1944.8 1760.5 184.2 9.6 0.9 5.9 0.04 0.01 1.5 0.09 17.3
6122-3 1130.3 1046.5 83.8 12.5 0.7 9.3 0.04 0.01 0.9 0.06 15.1
6122-11 1029.5 969.4 60.2 16.1 0.7 8.6 0.03 0.01 1.0 0.06 20.8
6122-12 928.0 859.4 68.6 12.5 0.5 11.7 0.04 0.01 0.8 0.05 16.0
6122-9 892.4 831.1 61.2 13.6 0.7 8.4 0.04 0.01 1.1 0.07 16.8
6122-2 852.3 768.6 83.6 9.2 0.7 6.0 0.06 0.01 1.0 0.09 9.7
6122-13 833.5 766.4 67.1 11.4 0.7 8.3 0.05 0.01 0.8 0.07 13.0
6122-4 793.5 705.7 87.7 8.0 0.7 7.5 0.07 0.01 0.8 0.07 8.8
6122-5 792.4 725.7 66.7 10.9 0.6 10.4 0.04 0.01 0.8 0.05 13.8
6122-15 740.0 679.7 60.2 11.3 0.6 7.7 0.04 0.01 1.0 0.07 15.1
6122-8 703.3 648.7 54.5 11.9 0.7 7.9 0.05 0.01 0.8 0.07 13.3
6122-6 655.1 605.4 49.7 12.2 0.7 10.0 0.03 0.01 1.3 0.05 19.4
6122-7 520.3 479.5 40.8 11.8 0.7 7.6 0.05 0.01 0.8 0.07 12.1
6139-2 3739.3 3398.1 341.2 10.0 0.6 8.5 0.03 0.01 1.4 0.06 18.8
6139-3 3838.3 3488.2 350.1 10.0 0.6 10.2 0.03 0.01 1.2 0.05 18.8
6139-4 4263.4 3969.5 293.9 13.5 0.7 13.5 0.02 0.01 1.2 0.04 24.8
6139-5 3187.3 2864.2 323.1 8.9 0.6 6.3 0.04 0.01 1.4 0.09 14.4
6139-6 4860.8 4432.6 428.2 10.4 0.7 8.7 0.04 0.01 1.2 0.06 15.6
6139-7 3309.8 2974.1 335.7 8.9 0.7 6.8 0.04 0.01 1.5 0.08 16.8
6139-8 2721.1 2412.9 308.2 7.8 0.7 6.9 0.05 0.01 1.3 0.08 13.3
6139-9 3590.9 3197.6 393.3 8.1 0.6 6.5 0.04 0.01 1.4 0.08 14.6
6139-11 1877.7 1564.2 313.5 5.0 0.7 6.2 0.10 0.02 0.8 0.09 6.1
250

APPENDIX D
Electron microprobe analyses of various chlorite phases from deposits of the Beaverlodge area
SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2O 3 FeO MnO MgO CaO NA 2O K 2O F CL H 2O O=F O=CL Total Temp ( o ) ±
RETROGRADE LOWER GREENSCHIST CHLORITE (Cl1)
Cl48-7 29.83 0.00 14.82 0.06 19.52 0.07 18.82 0.30 0.02 0.01 0.55 0.00 10.94 -0.23 0.00 94.71 197
Cl48-3 30.10 0.00 15.68 0.02 19.23 0.15 19.74 0.15 0.00 0.00 0.34 0.00 11.30 -0.14 0.00 96.56 211
Cl48-5 29.61 0.01 15.56 0.00 18.54 0.12 19.33 0.16 0.00 0.00 0.44 0.00 11.04 -0.19 0.00 94.63 210
Cl48 30.92 0.00 13.81 0.00 19.72 0.13 20.51 0.12 0.04 0.02 0.51 0.00 11.20 -0.21 0.00 96.77 183
Cl48-2-1 30.79 0.01 14.36 0.00 20.22 0.10 20.28 0.00 0.01 0.01 0.42 0.00 11.30 -0.18 0.00 97.32 192
AVG 30.25 0.00 14.85 0.02 19.45 0.11 19.74 0.15 0.01 0.01 0.45 0.00 11.16 -0.19 0.00 96.00 199 14
EARLY TENSIONAL VEINS URANIUM MINERALIZATION (Cl4)
6122_pt1-2-Cl 29.99 0.02 25.80 0.00 12.16 0.15 18.28 0.28 0.46 0.11 0.17 0.12 12.23 -0.07 -0.03 100.12 287
6122_pt2-1 27.23 -0.01 21.92 0.06 15.36 0.17 17.80 1.88 0.21 0.09 0.50 0.20 11.29 -0.21 -0.05 96.79 318
6122_pt3-2 27.70 -0.01 22.82 0.07 16.71 0.07 19.24 0.37 0.10 0.03 0.16 0.07 11.83 -0.07 -0.02 99.34 329
6122_pt4-1 25.53 0.00 19.50 0.04 11.47 0.22 14.11 10.29 0.44 0.57 0.87 0.10 10.55 -0.37 -0.02 93.71 329
6122_pt4-2 27.34 0.03 19.66 0.09 15.16 0.16 15.72 4.54 0.19 0.73 0.32 0.14 11.07 -0.13 -0.03 95.44 288
AVG 27.56 0.00 21.94 0.05 14.17 0.15 17.03 3.47 0.28 0.31 0.40 0.13 11.39 -0.17 -0.03 97.08 310 21
METASOMATIC -TYPE URANIUM MINERALIZATION (Cl5 Cl6)
Early Chlorite associated with the metasomatic type uranium mineralization (Cl 5 )
Gn21-1 26.65 0.07 19.29 0.00 20.31 0.37 17.80 0.01 0.04 0.02 0.31 0.00 11.11 -0.13 0.00 95.85 312
Gn21-2 26.97 0.05 19.13 0.00 20.39 0.41 18.56 0.00 0.01 0.00 0.23 0.00 11.28 -0.10 0.00 96.93 312
Gn21-4 26.63 0.08 19.71 0.01 20.98 0.37 17.83 0.01 0.00 0.01 0.19 0.00 11.28 -0.08 0.00 97.02 321
Gn21-5 27.24 0.04 19.64 0.00 20.61 0.43 18.17 0.02 0.01 0.00 0.26 0.00 11.35 -0.11 0.00 97.66 310
Gn21-6 26.70 0.07 19.27 0.00 20.62 0.32 18.49 0.00 0.03 0.02 0.29 0.00 11.23 -0.12 0.00 96.92 319
AVG 26.84 0.06 19.41 0.00 20.58 0.38 18.17 0.01 0.02 0.01 0.26 0.00 11.25 -0.11 0.00 96.88 315 6
Late Chlorite vein injected during late stage of the metasomatic process (Cl 6 )
GN03A-1 28.80 0.00 19.65 0.05 15.94 0.30 21.12 0.04 0.02 0.01 0.33 0.00 11.63 -0.14 0.00 97.75 282
GN03A-2 28.96 0.00 19.17 0.13 15.75 0.23 22.08 0.03 0.00 0.01 0.30 0.00 11.70 -0.13 0.00 98.24 282
GN03A-3 29.57 0.00 19.12 0.03 14.20 0.16 23.41 0.03 0.00 0.00 0.40 0.00 11.80 -0.17 0.00 98.55 273
GN03A-4 29.04 0.01 19.17 0.04 13.61 0.21 23.66 0.03 0.01 0.00 0.39 0.00 11.71 -0.16 0.00 97.72 284
251

SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2O 3 FeO MnO MgO CaO NA 2O K 2O F CL H 2O O=F O=CL Total Temp ( o ) ±
GN03A-5 29.38 0.04 19.27 0.06 15.61 0.28 21.65 0.03 0.01 0.01 0.37 0.00 11.70 -0.16 0.00 98.25 270
AVG 29.15 0.01 19.28 0.06 15.02 0.24 22.38 0.03 0.01 0.01 0.36 0.00 11.71 -0.15 0.00 98.10 278 7
Variably Altered Early Chlorite associated with the metasomatic type uranium mineralization
Gn12-2-1 28.49 0.02 18.10 0.04 21.32 0.32 17.40 0.06 0.00 0.01 0.24 0.00 11.29 -0.10 0.00 97.19 262
Gn12-2-2 30.37 0.02 16.57 0.00 15.18 0.11 23.61 0.04 0.01 0.00 0.54 0.00 11.57 -0.23 0.00 97.80 235
Gn12-4-1 28.75 0.02 17.17 0.03 19.96 0.35 18.47 0.09 0.02 0.01 0.32 0.00 11.20 -0.13 0.00 96.26 248
Gn12-4-2 29.73 0.00 16.20 0.01 15.10 0.07 23.53 0.03 0.02 0.00 0.44 0.00 11.44 -0.19 0.00 96.38 240
Gn12-6-1 28.45 0.01 18.10 0.02 21.14 0.25 17.19 0.04 0.01 0.02 0.41 0.00 11.16 -0.17 0.00 96.63 258
Gn12-6-2 30.76 0.01 16.18 0.01 14.14 0.16 24.14 0.01 0.02 0.01 0.26 0.00 11.71 -0.11 0.00 97.30 222
Gn12-8-1 28.47 0.02 18.13 0.01 20.59 0.28 17.35 0.05 0.02 0.01 0.44 0.00 11.14 -0.19 0.00 96.32 257
Gn12-8-2 29.91 0.03 16.13 0.00 14.29 0.14 23.05 0.02 0.02 0.01 0.52 0.00 11.31 -0.22 0.00 95.21 226
Gn12-101 28.49 0.00 17.60 0.02 21.33 0.34 17.90 0.08 0.06 0.03 0.43 0.00 11.20 -0.18 0.00 97.30 261
Gn12-102 30.44 0.02 15.97 0.00 14.54 0.15 23.99 0.00 0.02 0.01 0.25 0.00 11.64 -0.11 0.00 96.92 226
Gn12-111 29.03 0.01 17.49 0.03 19.76 0.34 19.08 0.05 0.08 0.04 0.57 0.00 11.25 -0.24 0.00 97.49 253
GN12-112 30.63 0.05 16.13 0.02 14.03 0.15 24.71 0.01 0.05 0.01 0.73 0.00 11.53 -0.31 0.00 97.74 230
GN-12-1 29.70 0.01 16.07 0.01 15.07 0.01 23.01 0.00 0.01 0.00 0.43 0.00 11.34 -0.18 0.00 95.48 233
AVG 29.48 0.02 16.65 0.02 16.95 0.20 21.74 0.03 0.04 0.02 0.48 0.00 11.39 -0.20 0.00 96.99 242 20
6140-1 29.88 0.00 15.97 0.04 18.10 0.05 20.83 0.03 0.01 0.01 0.27 0.00 11.38 -0.11 0.00 96.45 223
6140-2 29.88 0.00 15.97 0.04 18.10 0.05 20.83 0.03 0.01 0.01 0.27 0.00 11.38 -0.11 0.00 96.45 223
6140-3 29.29 0.01 15.94 0.06 19.97 0.04 20.34 0.01 0.01 0.02 0.38 0.00 11.29 -0.16 0.00 97.20 240
6140-4 29.46 0.02 16.05 0.02 18.31 0.07 20.84 0.03 0.02 0.05 0.27 0.00 11.34 -0.11 0.00 96.37 234
6140-5 29.18 0.01 15.56 0.01 19.32 0.05 20.19 0.03 0.01 0.01 0.34 0.00 11.17 -0.14 0.00 95.73 231
AVR 29.54 0.01 15.90 0.03 18.76 0.05 20.61 0.03 0.01 0.02 0.31 0.00 11.31 -0.13 0.00 96.44 230 8
6134_Pt2_Cl1 34.61 0.02 19.74 0.01 8.14 0.18 21.49 0.49 0.06 0.12 0.92 0.15 11.85 -0.39 -0.03 97.32 141
6134_Pt2_Cl2 35.20 -0.01 19.46 0.01 2.91 0.32 22.27 1.74 0.05 0.13 2.05 0.14 11.22 -0.86 -0.03 94.59 114
6134_Pt3_Cl1 36.06 0.01 20.00 0.03 3.53 0.30 21.07 0.97 0.06 0.17 1.01 0.11 11.78 -0.43 -0.02 94.62 92
6134_Pt4_Cl1 36.14 0.02 21.88 -0.01 4.59 0.25 20.48 0.92 0.04 0.27 1.56 0.06 11.82 -0.66 -0.01 97.62 116
AVG 35.50 0.01 20.27 0.01 4.79 0.26 21.33 1.03 0.05 0.17 1.38 0.11 11.67 -0.59 -0.02 96.04 116 24
BRECCIA-TYPE URANIUM MINERALIZATION (Cl7)
5812A-2 24.73 0.03 18.95 0.05 22.98 0.05 13.57 2.32 0.07 0.02 - 0.00 10.72 0.00 0.00 93.49 335
5812A-3 24.63 0.00 18.86 0.03 18.70 0.07 15.01 2.14 0.06 0.00 - 0.00 10.54 0.00 0.00 90.04 324
5812A-3-1 24.63 0.00 19.27 0.07 23.22 0.08 12.94 0.65 0.04 0.00 - 0.00 10.53 0.00 0.00 91.43 323
5812A-5-2 25.72 0.03 20.40 0.06 27.38 0.08 11.92 0.11 0.04 0.00 - 0.00 11.01 0.00 0.00 96.75 324
5812A-8-1 24.06 0.04 18.36 0.10 26.34 0.16 10.77 2.07 0.05 0.00 - 0.00 10.39 0.00 0.00 92.34 332
5812A-8-2 25.34 0.05 19.66 0.07 26.42 0.11 11.87 0.40 0.08 0.00 - 0.00 10.79 0.00 0.00 94.79 319
252

SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2O 3 FeO MnO MgO CaO NA 2O K 2O F CL H 2O O=F O=CL Total Temp ( o ) ±
5812A-8-3 25.65 0.04 20.38 0.02 27.32 0.07 11.90 0.17 0.02 0.00 - 0.00 10.99 0.00 0.00 96.56 324
5812A-9-1 25.68 0.03 19.84 0.08 27.38 0.08 11.78 0.24 0.03 0.00 - 0.00 10.91 0.00 0.00 96.05 317
5812A-9-2 25.24 0.01 19.56 0.08 28.15 0.09 11.44 0.08 0.05 0.00 - 0.00 10.79 0.00 0.00 95.49 323
5812A-10-1 25.83 0.02 20.21 0.10 27.24 0.05 12.54 0.20 0.03 0.00 - 0.00 11.08 0.00 0.00 97.30 325
5812A-10-2 24.97 0.04 19.24 0.08 26.38 0.06 11.97 1.92 0.04 0.00 - 0.00 10.81 0.00 0.00 95.51 334
5812-Pt1 25.93 0.01 21.15 0.05 27.87 0.02 12.65 0.77 0.04 0.03 0.28 0.04 11.20 -0.12 -0.01 100.18 343
5812-Pt2-2 25.21 0.01 20.87 0.23 25.78 0.07 13.46 0.31 0.02 0.01 0.08 0.02 11.06 -0.03 0.00 97.21 350
5812-Pt2-3 26.49 0.01 20.15 0.45 23.19 0.05 15.28 0.84 0.03 0.02 0.14 0.03 11.26 -0.01 -0.06 98.06 323
5812-Pt3-1 25.97 0.01 21.24 0.03 28.34 0.11 11.84 0.53 0.05 0.03 0.17 0.04 11.20 -0.07 -0.03 99.62 340
AVG 25.34 0.02 19.88 0.10 25.78 0.08 12.60 0.85 0.04 0.01 0.17 0.01 10.89 -0.02 -0.01 95.66 329 16
Late Chlorite replacement
C-27-221-1-1 30.08 0.06 16.42 0.00 15.04 0.14 22.66 0.10 0.00 0.00 0.52 0.00 11.39 -0.22 0.00 96.19 228
C-27-221-1-2 31.72 0.02 15.16 0.01 11.24 0.23 24.86 0.13 0.03 0.01 0.67 0.00 11.43 -0.28 0.00 95.23 183
C-27-221-1-3 31.62 0.00 15.04 0.00 11.23 0.14 24.82 0.12 0.01 0.01 0.48 0.00 11.46 -0.20 0.00 94.73 182
C-27-221-2-1 32.13 0.02 15.42 0.00 11.89 0.11 25.28 0.15 0.02 0.01 0.44 0.00 11.74 -0.19 0.00 97.02 188
C-27-221-3-1 30.84 0.03 15.16 0.00 11.33 0.13 24.02 0.15 0.01 0.01 0.49 0.00 11.26 -0.21 0.00 93.22 189
C-27-221-3-2 31.20 0.04 15.53 0.00 12.04 0.21 23.88 0.19 0.04 0.01 0.47 0.00 11.43 -0.20 0.00 94.84 192
AVG 31.27 0.03 15.46 0.00 12.13 0.16 24.25 0.14 0.02 0.01 0.51 0.00 11.45 -0.22 0.00 95.21 194 23
VOLCANIC-TYPE URANIUM MINERALIZATION (Cl8)
Chlorite associated with the volcanic-type uranium mineralization
C-27-319-1 26.62 0.01 18.11 0.02 28.73 0.00 13.53 0.02 0.01 0.00 0.04 0.00 11.08 -0.02 0.00 98.15 300
C-27-319-2 26.11 0.03 18.98 0.01 27.84 0.22 13.65 0.02 0.01 0.03 0.05 0.00 11.09 -0.02 0.00 98.02 319
C-27-319-3 26.14 0.02 18.78 0.04 28.87 0.21 12.99 0.01 0.00 0.06 0.07 0.00 11.04 -0.03 0.00 98.20 315
C-27-319-4 26.30 0.04 18.20 0.01 27.97 0.33 13.06 0.04 0.02 0.10 0.09 0.00 10.93 -0.04 0.00 97.05 301
C-27-319-5 25.97 0.00 18.38 0.02 28.32 0.23 13.37 0.01 0.00 0.01 0.08 0.00 10.95 -0.03 0.00 97.31 314
C-27-319-6-1 25.81 0.04 18.01 0.00 28.11 0.21 13.22 0.00 0.01 0.00 0.14 0.00 10.81 -0.06 0.00 96.30 309
C-27-319-6-2 25.89 0.05 18.48 0.04 28.39 0.26 13.19 0.00 0.02 0.01 0.10 0.00 10.94 -0.04 0.00 97.32 316
C-27-319-7 25.71 0.00 18.33 0.05 29.74 0.30 12.40 0.00 0.00 0.01 0.04 0.00 10.90 -0.02 0.00 97.47 317
AVG 26.07 0.02 18.41 0.02 28.50 0.22 13.18 0.01 0.01 0.03 0.08 0.00 10.97 -0.03 0.00 97.48 311 9
C-27-34-1 26.90 0.02 19.22 0.04 22.11 0.56 16.89 0.03 0.01 0.02 0.11 0.00 11.26 -0.05 0.00 97.12 308
C-27-34-2 26.19 0.00 19.43 0.00 22.61 0.48 16.48 0.01 0.02 0.02 0.16 0.00 11.12 -0.07 0.00 96.45 323
C-27-34-3 26.76 0.00 19.15 0.03 22.77 0.62 16.73 0.02 0.03 0.02 0.13 0.00 11.24 -0.05 0.00 97.45 312
C-27-34-4-1 26.94 0.02 19.22 0.05 22.45 0.53 17.11 0.02 0.01 0.00 0.11 0.00 11.32 -0.05 0.00 97.73 311
C-27-34-4-2 26.94 0.02 19.22 0.05 22.45 0.53 17.11 0.02 0.01 0.00 0.11 0.00 11.32 -0.05 0.00 97.73 311
C-27-34-5 26.62 0.01 19.28 0.03 22.33 0.58 16.93 0.00 0.01 0.01 0.10 0.00 11.24 0.00 -0.04 97.10 315
C-27-34-5-1 26.48 0.00 19.44 0.04 22.29 0.50 16.68 0.03 0.02 0.01 0.10 0.00 11.21 -0.04 0.00 96.75 317
253

SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2O 3 FeO MnO MgO CaO NA 2O K 2O F CL H 2O O=F O=CL Total Temp ( o ) ±
C-27-34-6 26.91 0.02 19.26 0.02 22.49 0.45 17.10 0.01 0.03 0.03 0.10 0.00 11.32 -0.04 0.00 97.70 312
CL57-4 26.17 0.02 17.82 0.02 27.91 0.34 14.34 0.03 0.01 0.01 0.00 0.00 11.05 0.00 0.00 97.72 311
AVG 26.66 0.01 19.12 0.03 23.05 0.51 16.60 0.02 0.02 0.01 0.10 0.00 11.23 -0.04 0.00 97.31 313 7
CL29-7 25.35 0.02 20.07 0.01 25.65 0.30 14.51 0.01 0.03 0.02 0.13 0.00 11.04 -0.05 0.00 97.09 344
CL29-8 25.98 0.00 19.20 0.00 24.85 0.24 15.10 0.03 0.03 0.02 0.20 0.00 11.00 -0.08 0.00 96.56 322
CL29-2 25.02 0.05 20.14 0.03 25.75 0.24 14.62 0.02 0.03 0.02 0.09 0.00 11.04 -0.04 0.00 97.01 354
CL29-4 25.69 0.04 19.48 0.02 26.21 0.26 14.58 0.00 0.03 0.05 0.11 0.11 11.04 -0.05 -0.02 97.55 334
CL29-5 25.71 0.03 19.39 0.02 25.97 0.21 14.97 0.02 0.02 0.08 0.18 0.00 11.06 -0.08 0.00 97.58 335
AVG 26.10 0.09 18.79 0.01 25.65 0.24 15.13 0.02 0.03 0.03 0.18 0.01 11.03 -0.07 0.00 97.22 338 16
Variably altered chlorite associated with the volcanic type uranium mineralization
CL57-1 29.61 0.00 15.65 0.03 22.37 0.30 18.39 0.12 0.06 0.02 - 0.00 11.44 0.00 0.00 97.99 226
CL57-2 28.68 0.00 15.68 0.11 24.13 0.35 17.64 0.08 0.03 0.03 - 0.00 11.32 0.00 0.00 98.05 248
CL57-3 29.09 0.02 15.85 0.02 23.57 0.27 18.20 0.19 0.02 0.02 - 0.00 11.44 0.00 0.00 98.69 244
CL57-5 29.75 0.00 14.72 0.01 21.98 0.30 18.68 0.17 0.07 0.01 - 0.00 11.33 0.00 0.00 97.02 212
CL57-6 29.95 0.00 14.99 0.10 20.00 0.23 18.76 0.17 0.04 0.01 - 0.00 11.28 0.00 0.00 95.53 200
CL57-7 29.25 0.00 15.05 0.07 22.45 0.23 18.27 0.10 0.08 0.02 - 0.00 11.27 0.00 0.00 96.79 224
CL29-6 27.98 0.08 16.00 0.02 26.42 0.19 15.18 0.04 0.03 0.01 0.19 0.00 10.99 -0.08 0.00 97.05 251
CL29-9 29.84 0.04 17.25 0.02 25.35 0.20 15.35 0.04 0.04 0.02 0.36 0.00 11.36 -0.15 0.00 99.72 227
AVG 29.27 0.02 15.65 0.05 23.28 0.26 17.56 0.11 0.05 0.02 0.28 0.00 11.30 -0.03 0.00 97.61 229 25
6139-3 27.66 0.02 17.39 0.06 25.32 0.22 11.81 0.37 0.18 0.34 0.00 0.00 10.79 0.00 0.00 94.16 236
6139-4 29.89 0.00 17.92 0.03 23.38 0.23 10.39 0.28 0.21 1.11 0.00 0.00 10.96 0.00 0.00 94.40 173
6139-5 27.52 0.05 17.48 0.05 25.20 0.26 11.60 0.28 0.18 0.33 0.00 0.00 10.74 0.00 0.00 93.69 236
6139-6 28.84 0.02 17.41 0.02 24.58 0.15 11.25 0.27 0.16 0.67 0.00 0.00 10.87 0.00 0.00 94.24 201
AVR 30.16 0.02 17.88 0.04 23.31 0.19 10.79 0.30 0.19 1.09 0.00 0.00 11.05 0.00 0.00 95.01 212 32
ATHABASCA-TYPE URANIUM MINERALIZATION Cl9)
3705-1 27.68 0.01 15.09 0.15 28.69 0.04 14.04 0.04 0.07 0.00 0.25 0.00 10.79 -0.11 0.00 96.74 246
3705-2 28.96 0.01 15.10 0.16 26.74 0.00 13.59 0.09 0.04 0.00 0.27 0.00 10.80 -0.11 0.00 95.65 203
3705-3 27.90 0.02 14.84 0.26 26.54 0.03 14.47 0.10 0.24 0.02 0.64 0.00 10.53 -0.27 0.00 95.33 232
3705-4 28.51 0.02 15.77 0.21 24.06 0.00 16.14 0.10 0.02 0.00 0.34 0.00 10.93 -0.14 0.00 95.96 234
3705-5 28.62 0.02 15.77 0.21 24.06 0.00 16.14 0.10 0.02 0.00 0.34 0.00 10.95 -0.14 0.00 96.09 231
3705-7 29.51 0.00 15.05 0.19 22.53 0.00 17.68 0.07 0.00 0.00 0.46 0.00 11.01 -0.19 0.00 96.31 211
3507_Pt1_Cl 28.33 0.04 15.78 0.19 27.49 0.02 15.30 0.07 0.01 0.02 0.31 0.11 11.03 -0.13 -0.02 99.23 250
3507_Pt2_Cl 28.43 0.02 15.55 0.11 26.61 -0.04 16.31 0.04 0.02 0.03 0.33 0.10 11.06 -0.14 -0.02 99.00 249
3507_Pt3_Cl 27.90 0.03 15.45 0.11 27.33 0.02 14.83 0.10 0.04 0.01 0.41 0.08 10.79 -0.17 -0.02 97.61 247
3507_Pt4_Cl 27.96 0.01 15.65 0.13 26.07 0.03 15.83 0.07 0.04 0.02 0.49 0.09 10.82 -0.21 -0.02 97.52 251
AVG 28.38 0.02 15.40 0.17 26.01 0.01 15.43 0.08 0.05 0.01 0.38 0.04 10.87 -0.16 -0.01 96.94 235 24
254

SAMPLE ID. SiO 2 TiO 2 AL 2O 3 CR 2O 3 FeO MnO MgO CaO NA 2O K 2O F CL H 2O O=F O=CL Total Temp ( o ) ±
LATE VEINS (Cl10)
6134_Pt2_Cl1 47.77 0.08 25.89 -0.02 11.16 0.01 2.21 0.69 0.15 5.90 0.13 0.08 4.25 -0.05 -0.02 99.08 161
6134_Pt2_Cl2 48.55 0.03 29.89 -0.02 4.33 0.01 3.75 0.20 0.27 7.02 - 0.07 4.45 -0.01 -0.02 98.92 179
6134_Pt3_Cl1 51.23 0.02 29.24 0.02 4.28 0.05 2.12 0.24 0.26 8.09
0.02
0.12 0.07 4.47 -0.05 -0.02 100.36 137
6134_Pt4_Cl1 48.47 0.02 23.70 -0.02 8.70 0.05 4.44 0.40 0.18 6.48 0.23 0.15 4.15 -0.03 -0.10 97.27 136
6134_Pt4_Cl2 48.14 0.20 21.84 0.01 10.41 0.03 2.42 0.75 0.18 6.20 0.30 0.03 4.01 -0.13 -0.01 94.99 108
AVG 48.83 0.07 26.11 -0.01 7.78 0.03 2.99 0.45 0.21 6.74 0.15 0.08 4.27 -0.05 -0.03 98.12 144
255

APPENDIX E
Electron microprobe data and temperatures of various chlorite phases from deposits of the Beaverlodge area
SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4+ Cr 3+ Fe 2+ Mn 2+ Mg 2+ Total Ca 2+ Na + K + Total F - CL - H + Total O 2- ∑Cat ∑ions
RETROGRADE LOWER GREENSCHIST CHLORITE (Cl1)
Cl48-7 3.20 0.81 4.00 1.87 0.00 0.01 1.75 0.01 3.01 6.64 0.03 0.00 0.00 0.04 0.19 0.00 7.81 8.00 17.81 9.87 18.00 197
Cl48-3 3.15 0.85 4.00 1.93 0.00 0.00 1.68 0.01 3.08 6.71 0.02 0.00 0.00 0.02 0.11 0.00 7.89 8.00 17.89 9.88 18.00 211
Cl48-5 3.16 0.84 4.00 1.96 0.00 0.00 1.65 0.01 3.07 6.69 0.02 0.00 0.00 0.02 0.15 0.00 7.85 8.00 17.85 9.87 18.00 210
Cl48 3.24 0.76 4.00 1.71 0.00 0.00 1.73 0.01 3.20 6.65 0.01 0.01 0.00 0.02 0.17 0.00 7.83 8.00 17.83 9.91 18.00 183
Cl48-2-1 3.21 0.79 4.00 1.77 0.00 0.00 1.76 0.01 3.15 6.69 0.00 0.00 0.00 0.00 0.14 0.00 7.86 8.00 17.86 9.91 18.00 192
AVG 3.19 0.81 4.00 1.85 0.00 0.00 1.72 0.01 3.10 6.68 0.02 0.00 0.00 0.02 0.15 0.00 7.85 8.00 17.85 9.89 18.00 199 14
EARLY TENSIONAL VEINS URANIUM MINERALIZATION (Cl4)
6122_pt1-2- 2.92 1.08 4.00 2.96 0.00 0.00 0.99 0.01 2.65 6.61 0.03 0.09 0.01 0.13 0.05 0.02 7.93 8.00 17.93 9.65 18.00 287
Cl
6122_pt2-1 2.82 1.18 4.00 2.68 0.00 0.01 1.33 0.02 2.75 6.78 0.21 0.04 0.01 0.26 0.16 0.04 7.80 8.00 17.80 9.86 18.00 318
6122_pt3-2 2.79 1.21 4.00 2.71 0.00 0.01 1.41 0.01 2.89 7.01 0.04 0.02 0.00 0.06 0.05 0.01 7.94 8.00 17.94 9.86 18.00 329
6122_pt4-1 2.79 1.21 4.00 2.51 0.00 0.00 1.05 0.02 2.30 5.88 1.20 0.09 0.08 1.38 0.30 0.02 7.68 8.00 17.68 10.04 18.00 329
6122_pt4-2 2.91 1.09 4.00 2.47 0.00 0.01 1.35 0.01 2.50 6.34 0.52 0.04 0.10 0.66 0.11 0.03 7.87 8.00 17.87 9.91 18.00 288
AVG 2.85 1.16 4.00 2.66 0.00 0.00 1.22 0.01 2.62 6.52 0.40 0.06 0.04 0.50 0.14 0.02 7.84 8.00 17.84 9.87 18.00 310 21
METASOMATIC -TYPE URANIUM MINERALIZATION (Cl5 Cl6)
Early chlorite associated with the metasomatic type uranium mineralization (Cl5)
Gn21-1 2.84 1.16 4.00 2.42 0.01 0.00 1.81 0.03 2.83 7.10 0.00 0.01 0.00 0.01 0.10 0.00 7.90 8.00 17.90 9.95 18.00 312
Gn21-2 2.84 1.16 4.00 2.38 0.00 0.00 1.80 0.04 2.91 7.12 0.00 0.00 0.00 0.00 0.08 0.00 7.93 8.00 17.93 9.97 18.00 312
Gn21-4 2.81 1.19 4.00 2.45 0.01 0.00 1.85 0.03 2.80 7.15 0.00 0.00 0.00 0.00 0.06 0.00 7.94 8.00 17.94 9.96 18.00 321
Gn21-5 2.85 1.15 4.00 2.42 0.00 0.00 1.80 0.04 2.83 7.09 0.00 0.00 0.00 0.00 0.09 0.00 7.91 8.00 17.91 9.94 18.00 310
Gn21-6 2.82 1.18 4.00 2.40 0.01 0.00 1.82 0.03 2.91 7.16 0.00 0.01 0.00 0.01 0.10 0.00 7.90 8.00 17.90 9.98 18.00 319
AVG 2.83 1.17 4.00 2.41 0.01 0.00 1.82 0.03 2.86 7.12 0.00 0.00 0.00 0.01 0.09 0.00 7.92 8.00 17.92 9.96 18.00 315 6
Late chlorite vein injected during late stage of the metasomatic process (Cl6)
GN03A-1 2.93 1.07 4.00 2.36 0.00 0.00 1.36 0.03 3.21 6.95 0.00 0.00 0.00 0.01 0.11 0.00 7.89 8.00 17.89 9.89 18.00 282
GN03A-2 2.93 1.07 4.00 2.29 0.00 0.01 1.33 0.02 3.33 6.98 0.00 0.00 0.00 0.00 0.10 0.00 7.90 8.00 17.90 9.92 18.00 282
GN03A-3 2.96 1.04 4.00 2.26 0.00 0.00 1.19 0.01 3.49 6.95 0.00 0.00 0.00 0.00 0.13 0.00 7.87 8.00 17.87 9.91 18.00 273
GN03A-4 2.93 1.07 4.00 2.28 0.00 0.00 1.15 0.02 3.56 7.00 0.00 0.00 0.00 0.01 0.12 0.00 7.88 8.00 17.88 9.93 18.00 284
GN03A-5 2.97 1.03 4.00 2.29 0.00 0.01 1.32 0.02 3.26 6.91 0.00 0.00 0.00 0.01 0.12 0.00 7.88 8.00 17.88 9.88 18.00 270
AVG 2.94 1.06 4.00 2.29 0.00 0.00 1.27 0.02 3.37 6.96 0.00 0.00 0.00 0.01 0.11 0.00 7.89 8.00 17.89 9.91 18.00 278 7
Variably altered early chlorite associated with the metasomatic type uranium mineralization
Temp
( o )
±
256

SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4+ Cr 3+ Fe 2+ Mn 2+ Mg 2+ Total Ca 2+ Na + K + Total F - CL - H + Total O 2- ∑Cat ∑ions
Gn12-2-1 3.00 1.01 4.00 2.24 0.00 0.00 1.87 0.03 2.73 6.88 0.01 0.00 0.00 0.01 0.08 0.00 7.92 8.00 17.92 9.88 18.00 262
Gn12-2-2 3.08 0.92 4.00 1.98 0.00 0.00 1.29 0.01 3.57 6.85 0.00 0.00 0.00 0.01 0.17 0.00 7.83 8.00 17.83 9.93 18.00 235
Gn12-4-1 3.04 0.96 4.00 2.14 0.00 0.00 1.76 0.03 2.91 6.84 0.01 0.00 0.00 0.02 0.11 0.00 7.89 8.00 17.89 9.90 18.00 248
Gn12-4-2 3.06 0.94 4.00 1.97 0.00 0.00 1.30 0.01 3.61 6.89 0.00 0.00 0.00 0.01 0.14 0.00 7.86 8.00 17.86 9.96 18.00 240
Gn12-6-1 3.01 0.99 4.00 2.25 0.00 0.00 1.87 0.02 2.71 6.85 0.01 0.00 0.00 0.01 0.14 0.00 7.86 8.00 17.86 9.87 18.00 258
Gn12-6-2 3.12 0.88 4.00 1.93 0.00 0.00 1.20 0.01 3.65 6.79 0.00 0.00 0.00 0.01 0.08 0.00 7.92 8.00 17.92 9.92 18.00 222
Gn12-8-1 3.01 0.99 4.00 2.26 0.00 0.00 1.82 0.03 2.73 6.84 0.01 0.00 0.00 0.01 0.15 0.00 7.85 8.00 17.85 9.86 18.00 257
Gn12-8-2 3.11 0.90 4.00 1.97 0.00 0.00 1.24 0.01 3.57 6.80 0.00 0.00 0.00 0.01 0.17 0.00 7.83 8.00 17.82 9.91 18.00 226
Gn12-101 3.00 1.00 4.00 2.18 0.00 0.00 1.88 0.03 2.81 6.90 0.01 0.01 0.00 0.03 0.14 0.00 7.86 8.00 17.86 9.92 18.00 261
Gn12-102 3.11 0.89 4.00 1.92 0.00 0.00 1.24 0.01 3.65 6.83 0.00 0.00 0.00 0.01 0.08 0.00 7.92 8.00 17.92 9.94 18.00 226
Gn12-111 3.02 0.98 4.00 2.15 0.00 0.00 1.72 0.03 2.96 6.86 0.01 0.02 0.01 0.03 0.19 0.00 7.81 8.00 17.81 9.91 18.00 253
GN12-112 3.09 0.91 4.00 1.92 0.00 0.00 1.19 0.01 3.72 6.84 0.00 0.01 0.00 0.01 0.23 0.00 7.77 8.00 17.77 9.95 18.00 230
GN-12-1 3.09 0.92 4.00 1.97 0.00 0.00 1.31 0.00 3.56 6.84 0.00 0.00 0.00 0.00 0.14 0.00 7.86 8.00 17.86 9.93 18.00 233
AVG 3.06 0.94 4.00 2.03 0.00 0.00 1.47 0.02 3.34 6.85 0.00 0.01 0.00 0.01 0.16 0.00 7.84 8.00 17.84 9.93 18.00 242 20
6140-1 3.11 0.89 4.00 1.96 0.00 0.00 1.58 0.00 3.24 6.78 0.00 0.00 0.00 0.01 0.09 0.00 7.91 8.00 17.91 9.91 18.00 223
6140-2 3.11 0.89 4.00 1.96 0.00 0.00 1.58 0.00 3.24 6.78 0.00 0.00 0.00 0.01 0.09 0.00 7.91 8.00 17.91 9.91 18.00 223
6140-3 3.06 0.94 4.00 1.96 0.00 0.01 1.75 0.00 3.17 6.89 0.00 0.00 0.00 0.01 0.13 0.00 7.87 8.00 17.87 9.96 18.00 240
6140-4 3.08 0.92 4.00 1.98 0.00 0.00 1.60 0.01 3.25 6.84 0.00 0.00 0.01 0.01 0.09 0.00 7.91 8.00 17.91 9.93 18.00 234
6140-5 3.09 0.91 4.00 1.94 0.00 0.00 1.71 0.00 3.19 6.84 0.00 0.00 0.00 0.01 0.11 0.00 7.89 8.00 17.89 9.94 18.00 231
AVR 3.09 0.91 4.00 1.96 0.00 0.00 1.64 0.00 3.22 6.83 0.00 0.00 0.00 0.01 0.10 0.00 7.90 8.00 17.90 9.93 18.00 230 8
6134_Pt2_Cl1 3.37 0.63 4.00 2.27 0.00 0.00 0.66 0.02 3.12 6.06 0.05 0.01 0.02 0.08 0.28 0.03 7.69 8.00 17.69 9.51 18.00 141
6134_Pt2_Cl2 3.45 0.55 4.00 2.25 0.00 0.00 0.24 0.03 3.26 5.77 0.18 0.01 0.02 0.21 0.64 0.02 7.34 8.00 17.34 9.43 18.00 114
6134_Pt3_Cl1 3.52 0.48 4.00 2.30 0.00 0.00 0.29 0.03 3.07 5.69 0.10 0.01 0.02 0.13 0.31 0.02 7.67 8.00 17.67 9.34 18.00 92
6134_Pt4_Cl1 3.45 0.55 4.00 2.46 0.00 0.00 0.37 0.02 2.91 5.76 0.09 0.01 0.03 0.13 0.47 0.01 7.52 8.00 17.52 9.34 18.00 116
AVG 3.45 0.55 4.00 2.32 0.00 0.00 0.39 0.02 3.09 5.82 0.11 0.01 0.02 0.14 0.43 0.02 7.56 8.00 17.56 9.41 18.00 116 24
BRECCIA-TYPE URANIUM MINERALIZATION (Cl7)
5812A-2 2.77 1.23 4.00 2.50 0.00 0.00 2.15 0.01 2.26 6.93 0.28 0.02 0.00 0.30 0.00 0.00 8.00 8.00 18.00 9.99 18.00 335
5812A-3 2.80 1.20 4.00 2.53 0.00 0.00 1.78 0.01 2.55 6.86 0.26 0.01 0.00 0.27 0.00 0.00 8.00 8.00 18.00 9.94 18.00 324
5812A-3-1 2.81 1.20 4.00 2.59 0.00 0.01 2.21 0.01 2.20 7.01 0.08 0.01 0.00 0.09 0.00 0.00 8.00 8.00 18.00 9.90 18.00 323
5812A-5-2 2.80 1.20 4.00 2.62 0.00 0.01 2.49 0.01 1.94 7.06 0.01 0.01 0.00 0.02 0.00 0.00 8.00 8.00 18.00 9.89 18.00 324
5812A-8-1 2.78 1.22 4.00 2.50 0.00 0.01 2.54 0.02 1.85 6.93 0.26 0.01 0.00 0.27 0.00 0.00 8.00 8.00 18.00 9.97 18.00 332
5812A-8-2 2.82 1.18 4.00 2.58 0.00 0.01 2.46 0.01 1.97 7.02 0.05 0.02 0.00 0.07 0.00 0.00 8.00 8.00 18.00 9.90 18.00 319
5812A-8-3 2.80 1.20 4.00 2.62 0.00 0.00 2.49 0.01 1.94 7.06 0.02 0.00 0.00 0.02 0.00 0.00 8.00 8.00 18.00 9.89 18.00 324
5812A-9-1 2.82 1.18 4.00 2.57 0.00 0.01 2.52 0.01 1.93 7.03 0.03 0.01 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.89 18.00 317
5812A-9-2 2.81 1.20 4.00 2.56 0.00 0.01 2.62 0.01 1.90 7.09 0.01 0.01 0.00 0.02 0.00 0.00 8.00 8.00 18.00 9.92 18.00 323
5812A-10-1 2.80 1.20 4.00 2.58 0.00 0.01 2.47 0.01 2.02 7.09 0.02 0.01 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.91 18.00 325
Temp
( o )
±
257

SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4+ Cr 3+ Fe 2+ Mn 2+ Mg 2+ Total Ca 2+ Na + K + Total F - CL - H + Total O 2- ∑Cat ∑ions
5812A-10-2 2.77 1.23 4.00 2.52 0.00 0.01 2.45 0.01 1.98 6.96 0.23 0.01 0.00 0.24 0.00 0.00 8.00 8.00 18.00 9.97 18.00 334
5812-Pt1 2.74 1.26 4.00 2.64 0.00 0.00 2.46 0.00 1.99 7.10 0.09 0.01 0.00 0.10 0.09 0.01 7.90 8.00 17.90 9.94 18.00 343
5812-Pt2-2 2.72 1.28 4.00 2.66 0.00 0.02 2.33 0.01 2.17 7.18 0.04 0.00 0.00 0.04 0.03 0.00 7.97 8.00 17.97 9.94 18.00 350
5812-Pt2-3 2.80 1.20 4.00 2.51 0.00 0.04 2.05 0.00 2.41 7.02 0.10 0.01 0.00 0.10 0.05 0.01 7.95 8.00 17.95 9.93 18.00 323
5812-Pt3-1 2.75 1.25 4.00 2.65 0.00 0.00 2.51 0.01 1.87 7.05 0.06 0.11 0.00 0.17 0.06 0.03 7.92 8.00 17.92 9.98 18.00 340
AVG 2.79 1.21 4.00 2.57 0.00 0.01 2.37 0.01 2.06 7.03 0.10 0.02 0.00 0.12 0.06 0.00 7.98 8.00 17.98 9.93 18.00 329 16
Late chlorite replacement
C-27-221-1-1 3.10 0.90 4.00 1.99 0.01 0.00 1.30 0.01 3.48 6.79 0.01 0.00 0.00 0.01 0.17 0.00 7.83 8.00 17.83 9.90 18.00 228
C-27-221-1-2 3.24 0.76 4.00 1.82 0.00 0.00 0.96 0.02 3.78 6.59 0.01 0.01 0.00 0.02 0.22 0.00 7.78 8.00 17.78 9.85 18.00 183
C-27-221-1-3 3.24 0.76 4.00 1.82 0.00 0.00 0.96 0.01 3.80 6.59 0.01 0.00 0.00 0.02 0.16 0.00 7.84 8.00 17.84 9.85 18.00 182
C-27-221-2-1 3.23 0.78 4.00 1.82 0.00 0.00 1.00 0.01 3.78 6.62 0.02 0.00 0.00 0.02 0.14 0.00 7.86 8.00 17.86 9.86 18.00 188
C-27-221-3-1 3.22 0.78 4.00 1.87 0.00 0.00 0.99 0.01 3.74 6.61 0.02 0.00 0.00 0.02 0.16 0.00 7.84 8.00 17.84 9.85 18.00 189
C-27-221-3-2 3.21 0.79 4.00 1.88 0.00 0.00 1.04 0.02 3.66 6.61 0.02 0.01 0.00 0.03 0.15 0.00 7.85 8.00 17.85 9.85 18.00 192
AVG 3.21 0.79 4.00 1.87 0.00 0.00 1.04 0.01 3.71 6.63 0.02 0.00 0.00 0.02 0.17 0.00 7.83 8.00 17.83 9.86 18.00 194 23
VOLCANIC-TYPE URANIUM MINERALIZATION (Cl8)
Chlorite associated with the volcanic-type uranium mineralization
C-27-319-1 2.88 1.12 4.00 2.31 0.00 0.00 2.60 0.00 2.18 7.09 0.00 0.00 0.00 0.00 0.01 0.00 7.99 8.00 17.99 9.97 18.00 300
C-27-319-2 2.82 1.18 4.00 2.42 0.00 0.00 2.51 0.02 2.20 7.15 0.00 0.00 0.00 0.01 0.02 0.00 7.98 8.00 17.98 9.97 18.00 319
C-27-319-3 2.83 1.17 4.00 2.40 0.00 0.00 2.61 0.02 2.10 7.13 0.00 0.00 0.01 0.01 0.02 0.00 7.98 8.00 17.98 9.97 18.00 315
C-27-319-4 2.87 1.13 4.00 2.34 0.00 0.00 2.56 0.03 2.13 7.06 0.01 0.00 0.01 0.02 0.03 0.00 7.97 8.00 17.97 9.96 18.00 301
C-27-319-5 2.83 1.17 4.00 2.36 0.00 0.00 2.59 0.02 2.18 7.15 0.00 0.00 0.00 0.00 0.03 0.00 7.97 8.00 17.97 9.98 18.00 314
C-27-319-6-1 2.85 1.15 4.00 2.34 0.00 0.00 2.59 0.02 2.17 7.13 0.00 0.00 0.00 0.00 0.05 0.00 7.95 8.00 17.95 9.98 18.00 309
C-27-319-6-2 2.83 1.17 4.00 2.38 0.00 0.00 2.59 0.02 2.15 7.15 0.00 0.00 0.00 0.01 0.04 0.00 7.97 8.00 17.97 9.98 18.00 316
C-27-319-7 2.82 1.18 4.00 2.37 0.00 0.00 2.73 0.03 2.03 7.17 0.00 0.00 0.00 0.00 0.01 0.00 7.99 8.00 17.99 9.99 18.00 317
AVG 2.84 1.16 4.00 2.36 0.00 0.00 2.60 0.02 2.14 7.13 0.00 0.00 0.00 0.01 0.03 0.00 7.97 8.00 17.97 9.98 18.00 311 9
C-27-34-1 2.85 1.15 4.00 2.40 0.00 0.00 1.96 0.05 2.67 7.09 0.00 0.00 0.00 0.01 0.04 0.00 7.96 8.00 17.96 9.95 18.00 308
C-27-34-2 2.81 1.19 4.00 2.45 0.00 0.00 2.03 0.04 2.63 7.16 0.00 0.00 0.00 0.01 0.05 0.00 7.95 8.00 17.95 9.97 18.00 323
C-27-34-3 2.84 1.16 4.00 2.39 0.00 0.00 2.02 0.06 2.65 7.12 0.00 0.01 0.00 0.01 0.04 0.00 7.96 8.00 17.96 9.97 18.00 312
C-27-34-4-1 2.84 1.16 4.00 2.39 0.00 0.00 1.98 0.05 2.69 7.12 0.00 0.00 0.00 0.00 0.04 0.00 7.96 8.00 17.96 9.96 18.00 311
C-27-34-4-2 2.84 1.16 4.00 2.39 0.00 0.00 1.98 0.05 2.69 7.12 0.00 0.00 0.00 0.00 0.04 0.00 7.96 8.00 17.96 9.96 18.00 311
C-27-34-5 2.83 1.17 4.00 2.41 0.00 0.00 1.98 0.05 2.68 7.14 0.00 0.00 0.00 0.00 0.00 - 7.97 7.93 17.97 9.97 18.00 315
C-27-34-5-1 2.82 1.18 4.00 2.44 0.00 0.00 1.99 0.05 2.65 7.13 0.00 0.00 0.00 0.01 0.03
0.03
0.00 7.97 8.00 17.97 9.96 18.00 317
C-27-34-6 2.84 1.16 4.00 2.40 0.00 0.00 1.99 0.04 2.69 7.11 0.00 0.01 0.00 0.01 0.03 0.00 7.97 8.00 17.97 9.97 18.00 312
CL57-4 2.84 1.16 4.00 2.28 0.00 0.00 2.53 0.03 2.32 7.17 0.00 0.00 0.00 0.01 0.00 0.00 8.00 8.00 18.00 10.02 18.00 311
AVG 2.83 1.17 4.00 2.40 0.00 0.00 2.05 0.05 2.63 7.13 0.00 0.00 0.00 0.01 0.03 0.00 7.97 7.99 17.97 9.97 18.00 313 7
Temp
( o )
±
258

SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4+ Cr 3+ Fe 2+ Mn 2+ Mg 2+ Total Ca 2+ Na + K + Total F - CL - H + Total O 2- ∑Cat ∑ions
CL29-7 2.74 1.26 4.00 2.56 0.00 0.00 2.32 0.03 2.34 7.24 0.00 0.01 0.00 0.01 0.04 0.00 7.96 8.00 17.96 9.99 18.00 344
CL29-8 2.81 1.19 4.00 2.45 0.00 0.00 2.25 0.02 2.43 7.15 0.00 0.01 0.00 0.01 0.07 0.00 7.93 8.00 17.93 9.97 18.00 322
CL29-2 2.71 1.29 4.00 2.57 0.00 0.00 2.33 0.02 2.36 7.29 0.00 0.01 0.00 0.01 0.03 0.00 7.97 8.00 17.97 10.01 18.00 354
CL29-4 2.77 1.23 4.00 2.48 0.00 0.00 2.36 0.02 2.34 7.21 0.00 0.01 0.01 0.01 0.04 - 7.94 7.96 17.94 10.00 18.00 334
CL29-5 2.77 1.23 4.00 2.46 0.00 0.00 2.34 0.02 2.40 7.22 0.00 0.00 0.01 0.02 0.06
0.02
0.00 7.94 8.00 17.94 10.01 18.00 335
AVG 2.81 1.19 4.00 2.39 0.01 0.00 2.31 0.02 2.43 7.16 0.00 0.01 0.00 0.01 0.06 0.00 7.94 8.00 17.94 9.99 18.00 338 16
Variably altered chlorite associated with the volcanic type uranium mineralization
CL57-1 3.11 0.90 4.00 1.93 0.00 0.00 1.96 0.03 2.88 6.80 0.01 0.01 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.93 18.00 226
CL57-2 3.04 0.96 4.00 1.96 0.00 0.01 2.14 0.03 2.79 6.92 0.01 0.01 0.00 0.02 0.00 0.00 8.00 8.00 18.00 9.98 18.00 248
CL57-3 3.05 0.95 4.00 1.96 0.00 0.00 2.07 0.02 2.84 6.90 0.02 0.00 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.97 18.00 244
CL57-5 3.15 0.85 4.00 1.84 0.00 0.00 1.95 0.03 2.95 6.76 0.02 0.01 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.94 18.00 212
CL57-6 3.19 0.82 4.00 1.88 0.00 0.01 1.78 0.02 2.97 6.66 0.02 0.01 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.88 18.00 200
CL57-7 3.11 0.89 4.00 1.89 0.00 0.01 2.00 0.02 2.90 6.81 0.01 0.02 0.00 0.03 0.00 0.00 8.00 8.00 18.00 9.95 18.00 224
CL29-6 3.03 0.97 4.00 2.04 0.01 0.00 2.39 0.02 2.45 6.91 0.01 0.01 0.00 0.01 0.07 0.00 7.94 8.00 17.94 9.95 18.00 251
CL29-9 3.10 0.90 4.00 2.11 0.00 0.00 2.21 0.02 2.38 6.72 0.00 0.01 0.00 0.02 0.12 0.00 7.88 8.00 17.88 9.84 18.00 227
AVG 3.10 0.90 4.00 1.95 0.00 0.00 2.06 0.02 2.77 6.81 0.01 0.01 0.00 0.02 0.02 0.00 7.98 8.00 17.98 9.93 18.00 229 25
6139-3 3.08 0.93 4.00 2.28 0.00 0.01 2.35 0.02 1.96 6.62 0.04 0.04 0.05 0.13 0.00 0.00 8.00 8.00 18.00 9.83 18.00 236
6139-4 3.27 0.73 4.00 2.31 0.00 0.00 2.14 0.02 1.70 6.17 0.03 0.05 0.16 0.23 0.00 0.00 8.00 8.00 18.00 9.67 18.00 173
6139-5 3.07 0.93 4.00 2.30 0.00 0.00 2.35 0.03 1.93 6.62 0.03 0.04 0.05 0.12 0.00 0.00 8.00 8.00 18.00 9.81 18.00 236
6139-6 3.18 0.82 4.00 2.27 0.00 0.00 2.27 0.01 1.85 6.40 0.03 0.03 0.09 0.16 0.00 0.00 8.00 8.00 18.00 9.75 18.00 201
AVR 3.27 0.73 4.00 2.29 0.00 0.00 2.12 0.02 1.75 6.18 0.03 0.04 0.15 0.22 0.00 0.00 8.00 8.00 18.00 9.68 18.00 212 32
ATHABASCA-TYPE URANIUM MINERALIZATION (Cl9)
3705-1 3.04 0.96 4.00 1.96 0.00 0.01 2.64 0.00 2.30 6.92 0.01 0.02 0.00 0.02 0.09 0.00 7.91 8.00 17.91 9.98 18.00 246
3705-2 3.18 0.82 4.00 1.95 0.00 0.01 2.45 0.00 2.22 6.65 0.01 0.01 0.00 0.02 0.09 0.00 7.91 8.00 17.91 9.84 18.00 203
3705-3 3.09 0.91 4.00 1.94 0.00 0.02 2.46 0.00 2.39 6.81 0.01 0.05 0.00 0.07 0.22 0.00 7.78 8.00 17.78 9.96 18.00 232
3705-4 3.08 0.92 4.00 2.01 0.00 0.02 2.18 0.00 2.60 6.81 0.01 0.00 0.00 0.02 0.12 0.00 7.88 8.00 17.88 9.90 18.00 234
3705-5 3.09 0.91 4.00 2.01 0.00 0.02 2.17 0.00 2.60 6.80 0.01 0.00 0.00 0.02 0.12 0.00 7.88 8.00 17.88 9.90 18.00 231
3705-7 3.15 0.85 4.00 1.89 0.00 0.02 2.01 0.00 2.81 6.74 0.01 0.00 0.00 0.01 0.16 0.00 7.85 8.00 17.85 9.89 18.00 211
3507_Pt1_Cl 3.03 0.97 4.00 1.99 0.00 0.02 2.46 0.00 2.44 6.91 0.01 0.00 0.00 0.01 0.11 0.02 7.88 8.00 17.88 9.96 18.00 250
3507_Pt2_Cl 3.03 0.97 4.00 1.96 0.00 0.01 2.37 0.00 2.59 6.94 0.01 0.00 0.00 0.01 0.11 0.02 7.87 8.00 17.87 9.99 18.00 249
3507_Pt3_Cl 3.04 0.96 4.00 1.99 0.00 0.01 2.49 0.00 2.41 6.90 0.01 0.01 0.00 0.02 0.14 0.02 7.84 8.00 17.84 9.96 18.00 247
3507_Pt4_Cl 3.03 0.97 4.00 2.00 0.00 0.01 2.36 0.00 2.56 6.93 0.00 0.01 0.00 0.01 0.17 0.02 7.82 8.00 17.82 9.97 18.00 251
AVG 3.08 0.92 4.00 1.97 0.00 0.01 2.36 0.00 2.49 6.84 0.01 0.01 0.00 0.02 0.13 0.01 7.86 8.00 17.86 9.94 18.00 235 24
LATE VEINS (Cl10)
6134_Pt2_Cl1 3.31 0.69 4.00 2.11 0.00 0.01 0.65 0.00 0.23 3.00 0.05 0.05 0.52 0.62 0.03 0.01 1.96 2.00 11.96 6.90 12.00 161
Temp
( o )
±
259

SAMPLE Si 4+ AL 4+ Total AL 6+ Ti 4+ Cr 3+ Fe 2+ Mn 2+ Mg 2+ Total Ca 2+ Na + K + Total F - CL - H + Total O 2- ∑Cat ∑ions
6134_Pt2_Cl2 3.25 0.75 4.00 2.36 0.00 0.00 0.24 0.00 0.37 2.98 0.01 0.04 0.60 0.65 0.00 1.99 1.99 11.99 6.88 12.00 179
6134_Pt3_Cl1 3.38 0.62 4.00 2.27 0.00 0.00 0.24 0.00 0.21 2.72 0.02 0.03 0.68 0.73 0.03 0.01 1.97 2.00 11.97 6.84 12.00 137
6134_Pt4_Cl1 3.38 0.62 4.00 1.95 0.00 0.00 0.51 0.00 0.46 2.93 0.03 0.02 0.58 0.63 0.05 0.02 1.93 2.00 11.93 6.94 12.00 136
6134_Pt4_Cl2 3.47 0.53 4.00 1.86 0.01 0.00 0.63 0.00 0.26 2.76 0.06 0.03 0.57 0.65 0.07 0.00 1.93 2.00 11.93 6.89 12.00 108
AVG 3.36 0.64 4.00 2.11 0.00 0.00 0.45 0.00 0.31 2.88 0.03 0.03 0.59 0.66 0.04 0.41 1.95 2.39 11.96 6.89 12.00 144
Temp
( o )
±
260

APPENDIX F
Results of the electron microprobe analyses for different uraninite occurrences in the Beaverlodge area: average
chemical composition and calculated chemical Pb age. Note: the composition is reported in weight percent and
the age in Ma
Sample ID. Deposit UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Chemical Pb
age (Ma)
Early tensional vein type-uraninite
6122_Pt2 1 Ace Fay 71.83 2.02 3.61 0.39 0.40 0.03 0.11 17.88 0.02 0.03 0.02 0.05 0.12 0.00 0.14 0.03 96.50 1544
6122_Pt3 1 Ace Fay 73.07 3.05 3.45 0.91 0.38 0.05 0.03 14.52 0.04 0.10 0.02 0.02 0.15 0.07 0.11 0.07 95.90 1233
6122_Pt4_2 Ace Fay 72.61 0.59 3.33 0.31 0.65 0.02 0.04 17.42 0.03 0.02 0.02 0.03 0.18 0.04 0.02 0.00 95.29 1488
6122_Pt5_1 Ace Fay 71.65 0.46 2.32 0.11 0.38 0.04 0.06 19.91 0.02 0.05 0.01 0.01 0.07 0.09 0.01 0.02 95.10 1724
6122_Pt10 1 Ace Fay 73.64 9.89 2.48 1.14 1.36 0.28 0.23 1.90 0.36 0.06 0.01 0.03 0.36 0.08 0.20 0.05 91.80 160
Gunnar type-uraninite
6134 pt2 1 Gunnar 77.59 3.01 5.35 0.15 0.06 0.01 0.04 0.07 0.12 0.14 0.01 0.01 0.03 0.02 0.07 0.04 86.61 5
6134 pt2 2 Gunnar 80.25 3.04 5.60 0.23 0.03 0.01 0.09 0.12 0.00 0.08 0.03 0.00 0.08 0.04 0.06 0.04 89.46 9
6134 pt2 3 Gunnar 78.63 3.65 5.19 1.65 0.33 0.01 0.06 0.00 0.06 0.07 0.02 0.02 0.06 0.00 0.07 0.12 89.78 0
6134 pt2 4 Gunnar 78.36 3.72 5.28 1.82 0.44 0.05 0.02 0.03 0.06 0.06 0.05 0.02 0.06 0.01 0.05 0.02 89.85 2
6134 pt3 Gunnar 77.88 4.95 5.57 0.19 0.37 0.01 0.01 0.12 0.05 0.07 0.03 0.01 0.09 0.01 0.08 0.01 89.33 9
6134 pt3 1 Gunnar 79.27 3.95 5.52 0.15 0.01 0.03 0.04 0.11 0.08 0.08 0.04 0.01 0.03 0.00 0.04 0.02 89.22 9
6134 pt3 2 Gunnar 81.64 3.39 4.56 0.16 0.00 0.12 0.07 0.03 0.05 0.06 0.04 0.00 0.07 0.03 0.08 0.05 90.13 2
6134 pt3 3 Gunnar 79.50 3.78 5.54 0.11 0.06 0.04 0.02 0.06 0.09 0.06 0.02 0.00 0.04 0.00 0.06 0.01 89.23 4
261

Sample ID. Deposit UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Chemical Pb
age (Ma)
6134 pt4 1 Gunnar 80.77 3.52 5.67 0.23 0.01 0.01 0.00 0.13 0.01 0.07 0.03 0.01 0.09 0.04 0.01 0.04 90.58 10
6134 pt4 2 Gunnar 79.52 3.13 5.90 0.26 0.13 0.01 0.03 0.09 0.07 0.05 0.00 0.03 0.07 0.01 0.03 0.01 89.31 7
6134 pt4 3 Gunnar 81.29 2.79 5.67 0.20 0.03 0.00 0.02 0.16 0.01 0.05 0.02 0.00 0.07 0.03 0.04 0.02 90.29 12
6134 pt5 1 Gunnar 81.39 2.70 5.41 0.13 0.00 0.04 0.00 0.11 0.04 0.06 0.07 0.00 0.05 0.06 0.02 0.07 89.88 8
6134 pt5 2 Gunnar 74.27 3.20 4.97 0.22 0.08 0.04 0.02 0.04 0.11 0.23 0.02 0.01 0.10 0.02 0.05 0.04 83.27 3
6134 pt5 3 Gunnar 80.12 4.95 4.54 0.22 0.41 0.01 0.01 0.10 0.12 0.12 0.05 0.01 0.02 0.16 0.01 0.01 90.75 8
6134 pt6 1 Gunnar 81.12 3.04 5.23 0.01 0.01 0.04 0.01 0.03 0.00 0.04 0.02 0.01 0.01 0.01 0.02 0.01 89.49 2
6134 pt6 2 Gunnar 81.92 3.06 5.25 0.04 0.04 0.00 0.00 0.10 0.01 0.04 0.02 0.00 0.08 0.04 0.04 0.04 90.45 7
6134 pt6 3 Gunnar 80.49 3.09 5.36 0.02 0.02 0.01 0.09 0.08 0.04 0.06 0.01 0.01 0.01 0.04 0.09 0.01 89.37 6
6134 pt6 4 Gunnar 81.96 3.12 4.98 0.05 0.04 0.01 0.02 0.10 0.02 0.06 0.04 0.00 0.07 0.02 0.01 0.01 90.44 8
6134 pt8 1 Gunnar 79.17 2.87 4.43 0.01 0.02 0.01 0.57 1.40 0.09 0.07 0.02 0.10 0.03 0.16 0.07 0.01 88.96 110
6134 pt8 2 Gunnar 79.67 2.90 4.69 0.02 0.07 0.03 0.35 1.44 0.06 0.00 0.03 0.07 0.02 0.08 0.10 0.05 89.42 112
6134 pt8 3 Gunnar 80.29 3.14 3.87 0.03 0.78 0.01 0.05 0.11 0.08 0.03 0.04 0.00 0.04 0.12 0.00 0.00 88.53 9
6134 pt8 4 Gunnar 77.08 2.76 5.44 0.05 0.02 0.02 0.53 0.61 0.09 0.01 0.01 0.04 0.06 0.21 0.02 0.04 86.86 49
6134 pt8a 1 Gunnar 80.50 4.02 5.50 0.04 0.11 0.02 0.00 0.07 0.01 0.12 0.06 0.02 0.07 0.05 0.03 0.00 90.45 5
6134 pt8a 2 Gunnar 82.92 2.92 5.30 0.07 0.04 0.02 0.09 0.11 0.01 0.07 0.01 0.04 0.10 0.01 0.07 0.02 91.62 8
6134 pt8a 3 Gunnar 77.51 1.83 5.81 0.17 0.02 0.02 0.05 0.16 0.11 0.15 0.00 0.03 0.12 0.01 0.06 0.07 85.99 13
6134 pt9 1 Gunnar 63.41 3.15 4.32 0.08 0.04 0.03 0.24 1.46 0.18 0.19 0.03 0.05 0.08 0.12 0.05 0.02 73.42 143
6134 pt9 2 Gunnar 75.28 3.78 5.33 0.02 0.07 0.01 0.29 1.41 0.22 0.08 0.00 0.03 0.01 0.20 0.02 0.07 86.69 117
6134 pt9 3 Gunnar 73.41 2.98 5.19 0.09 0.09 0.05 0.31 1.60 0.28 0.29 0.03 0.02 0.07 0.19 0.06 0.03 84.62 135
6134 pt9a 1 Gunnar 81.55 3.36 4.26 0.18 0.69 0.00 0.08 0.08 0.15 0.10 0.01 0.01 0.06 0.07 0.02 0.00 90.57 6
6134 pt9a 2 Gunnar 80.44 2.93 4.23 0.04 0.47 0.06 0.14 0.21 0.15 0.07 0.01 0.01 0.05 0.13 0.02 0.04 88.96 16
6134 pt9a 3 Gunnar 78.82 3.02 4.69 0.03 0.60 0.03 0.15 0.05 0.14 0.05 0.01 0.00 0.03 0.15 0.04 0.05 87.79 4
6134 pt9a 4 Gunnar 77.24 5.45 4.77 0.44 0.46 0.04 0.00 0.12 0.19 0.16 0.00 0.01 0.09 0.16 0.05 0.03 89.07 10
6134 pt10 1 Gunnar 73.83 6.55 3.47 1.32 0.01 0.03 0.07 0.41 0.09 0.14 0.00 0.01 0.05 0.27 0.01 0.06 86.09 35
6134 pt10 2 Gunnar 64.50 9.49 2.43 9.15 0.06 0.01 0.12 0.65 0.12 0.28 0.06 0.03 0.05 0.32 0.26 0.05 87.17 63
6134 pt10 3 Gunnar 74.14 7.47 3.23 1.59 0.01 0.01 0.06 0.32 0.04 0.16 0.00 0.01 0.01 0.27 0.03 0.04 87.34 27
6134 pt10 4 Gunnar 74.03 5.88 2.71 1.97 0.08 0.01 0.18 1.96 0.14 0.13 0.03 0.01 0.01 0.41 0.03 0.07 87.58 164
262

Sample ID. Deposit UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Chemical Pb
age (Ma)
6134 pt10 5 Gunnar 72.59 6.19 3.29 2.40 0.04 0.02 0.08 1.39 0.14 0.15 0.02 0.01 0.03 0.26 0.11 0.01 86.58 119
Breccia type-uraninite
5812 Pt1 1 Gunnar 75.59 0.50 4.51 0.62 0.46 0.03 0.18 12.07 0.02 0.04 0.03 0.01 0.42 0.45 0.08 0.05 94.92 991
5812 Pt6 2 Ace Fay 34.12 48.31 1.48 1.21 0.18 0.02 0.01 3.86 0.65 0.08 0.03 0.59 0.24 0.14 0.09 0.05 90.96 702
5812 Pt6 1 Ace Fay 74.88 0.54 4.43 0.44 0.44 0.01 0.16 15.88 0.02 0.03 0.02 0.01 0.22 0.15 0.04 0.00 97.16 1315
5812 Pt1 2 Ace Fay 76.71 0.98 6.43 0.90 0.61 0.03 0.21 6.89 0.01 0.03 0.04 0.06 0.70 0.60 0.00 0.01 94.18 557
5812 Pt8 1 Ace Fay 77.99 1.05 4.27 1.20 0.80 0.05 0.01 8.71 0.02 0.03 0.29 0.03 0.35 0.06 0.05 0.02 94.82 693
5812 Pt2 2 Ace Fay 75.02 2.40 4.63 1.28 1.74 0.01 0.14 10.07 0.05 0.06 0.03 0.73 0.67 0.31 0.11 0.03 97.15 832
Volcanic type-uraninite
6120B_pt4 2 Ace Fay 74.34 1.13 4.30 0.95 0.43 0.02 0.26 14.17 0.05 0.03 0.01 0.01 0.23 0.04 0.02 0.00 95.92 1183
6120B_pt3 1 Ace Fay 74.41 0.84 3.66 0.48 0.65 0.01 0.22 15.41 0.06 0.03 0.02 0.02 0.20 0.03 0.09 0.03 95.99 1285
6120B_pt3 2 Ace Fay 74.38 1.68 2.57 0.54 0.58 0.03 0.13 15.68 0.03 0.03 0.00 0.02 0.10 0.09 0.00 0.03 95.82 1307
6120B_pt2 2 Ace Fay 71.88 1.43 3.00 0.46 0.48 0.03 0.25 17.14 0.06 0.02 0.00 0.01 0.08 0.01 0.07 0.03 94.86 1479
6120B_pt1 2 Ace Fay 73.42 1.05 2.73 0.45 0.52 0.01 0.48 17.56 0.06 0.03 0.07 0.04 0.12 0.01 0.04 0.07 96.46 1484
6120B_pt3 3 Ace Fay 73.75 0.47 3.05 0.29 0.42 0.03 0.09 17.91 0.05 0.04 0.05 0.00 0.07 0.03 0.06 0.04 96.19 1506
6120B_pt5 2 Ace Fay 73.23 0.46 2.58 0.43 0.37 0.03 0.04 19.04 0.03 0.03 0.01 0.01 0.07 0.06 0.03 0.03 96.37 1613
6120B_pt6 1 Ace Fay 71.73 0.92 2.35 0.28 0.49 0.04 0.46 19.29 0.04 0.03 0.02 0.03 0.01 0.03 0.05 0.01 95.67 1668
6120B_pt3 4 Ace Fay 74.04 0.50 2.50 0.32 0.30 0.03 0.13 20.15 0.04 0.04 0.02 0.03 0.01 0.02 0.03 0.04 98.05 1689
6120B_pt5 1 Ace Fay 72.87 0.38 2.37 0.23 0.29 0.01 0.16 19.91 0.05 0.02 0.01 0.04 0.04 0.11 0.09 0.03 96.56 1695
6120B_pt4 1 Ace Fay 70.14 0.67 2.65 0.15 0.37 0.01 0.33 19.62 0.04 0.02 0.05 0.02 0.08 0.04 0.08 0.01 94.13 1735
6120B_pt4 1 Ace Fay 71.92 0.51 2.33 0.05 0.51 0.01 0.11 20.29 0.03 0.02 0.08 0.04 0.05 0.09 0.06 0.02 95.99 1750
Athabasca type-uraninite
3705 Pt4 5 Ace Fay 24.22 2.29 0.49 3.46 59.66 0.03 1.23 4.43 0.04 0.02 0.01 0.44 0.01 0.04 0.16 0.00 96.29 1135
3705 Pt3 2 Ace Fay 38.66 4.78 1.74 3.34 36.72 0.06 0.86 5.48 0.01 0.02 0.10 0.40 0.04 0.01 0.22 0.02 92.19 880
3705 Pt3 4 Ace Fay 39.64 6.95 1.09 4.31 36.08 0.04 0.62 3.14 0.30 0.04 0.07 0.00 0.02 0.02 0.07 0.06 92.29 492
3705 Pt4 2 Ace Fay 29.41 9.42 1.69 4.03 36.11 0.08 0.38 1.68 2.70 0.11 0.05 0.01 0.03 0.20 0.11 0.04 85.79 354
3705 Pt4 1 Ace Fay 48.08 10.87 2.67 3.29 16.60 0.00 0.33 5.69 0.84 0.13 0.15 0.86 0.04 0.44 0.20 0.07 89.96 735
263

Sample ID. Deposit UO 2 SiO 2 CaO Fe 2O 3 TiO 2 Cr 2O 3 V 2O 5 PbO P 2O 5 K 2O ThO 2 SO 2 MnO Y 2O 3 Tb 2O 3 CuO Total
Chemical Pb
age (Ma)
3705 Pt4 3 Ace Fay 28.39 8.87 2.09 6.23 44.41 0.02 0.62 2.17 0.18 0.10 0.02 0.01 0.04 0.03 0.26 0.00 93.18 473
3705 Pt2 7 Ace Fay 36.89 10.39 1.29 6.22 33.91 0.01 0.45 0.58 0.74 0.10 0.14 0.01 0.00 0.09 0.18 0.00 90.80 98
3705 Pt2 4 Ace Fay 34.12 11.57 1.16 5.91 33.49 0.01 0.32 0.71 0.77 0.11 0.10 0.01 0.01 0.06 0.10 0.04 88.37 130
3705 Pt4 7 Ace Fay 34.71 11.31 1.27 6.26 34.74 0.01 0.53 0.84 0.64 0.14 0.08 0.02 0.02 0.01 0.13 0.08 90.57 149
3705 Pt2 5 Ace Fay 35.07 11.45 1.29 6.67 36.99 0.01 0.57 0.76 0.61 0.08 0.04 0.00 0.06 0.04 0.15 0.02 93.68 135
3705 Pt4 6 Ace Fay 29.87 12.08 1.98 6.51 36.63 0.22 0.46 1.09 0.58 0.09 0.21 0.00 0.04 0.02 0.20 0.03 89.80 227
3705 Pt4 4 Ace Fay 41.88 16.19 0.63 3.07 28.28 0.01 0.97 0.78 0.30 0.01 0.14 0.00 0.02 0.08 0.12 0.05 92.38 116
3705 Pt2 6 Ace Fay 33.11 13.43 1.46 5.84 36.83 0.02 0.21 1.19 0.62 0.10 0.12 0.02 0.05 0.01 0.20 0.02 93.00 223
3705 Pt2 3 Ace Fay 39.04 16.30 0.64 3.39 28.73 0.07 1.15 0.74 0.30 0.02 0.04 0.01 0.02 0.06 0.10 0.03 90.50 117
3705 Pt3 1 Ace Fay 45.91 17.68 2.01 2.59 16.32 0.01 0.23 0.74 0.95 0.01 0.15 0.00 0.03 0.20 0.09 0.01 86.83 100
.
264

APPENDIX G
Isotopic data and apparent ages for various generations of uraninite from the South Alligator River area
Corrected ratios
Apparent ages ( ±1σ, Ma)**
Sample
Deposit
206 Pb/ 204 Pb
207 Pb/ 204 Pb
207 Pb/ 206 Pb ±2σ
206 Pb/ 238 U ±2σ
207 Pb/ 235 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
c29-217h Coronation Hill 6342 430 0.0678 0.001 0.0931 0.002 0.8695 0.023 0.92 862 15 574 14 635 13 26
c29-217d Coronation Hill 5944 399 0.0673 0.001 0.0932 0.006 0.8633 0.050 0.93 846 33 574 37 632 27 25
c29-217t Coronation Hill 7864 522 0.0665 0.001 0.0937 0.004 0.8598 0.039 0.92 823 29 578 26 630 21 23
c29-217m Coronation Hill 7218 487 0.0674 0.000 0.0942 0.004 0.8759 0.036 0.95 852 11 580 22 639 19 25
c29-217p Coronation Hill 4090 287 0.0701 0.001 0.0950 0.003 0.9185 0.025 0.85 931 28 585 16 662 13 29
c29-217za Coronation Hill 6129 408 0.0671 0.001 0.0954 0.008 0.8805 0.057 0.95 840 43 587 45 641 31 24
c29-217s Coronation Hill 3752 270 0.0722 0.002 0.0955 0.005 0.9487 0.030 0.87 990 49 588 28 677 16 32
C29-217b Coronation Hill 3122 219 0.0703 0.001 0.0967 0.004 0.9367 0.030 0.93 936 23 595 22 671 16 28
c29-217e Coronation Hill 6699 451 0.0675 0.001 0.0986 0.005 0.9178 0.052 0.80 854 42 606 32 661 27 23
c29-217f Coronation Hill 6466 438 0.0678 0.001 0.1009 0.003 0.9440 0.034 0.92 863 21 620 18 675 18 22
c29-217q Coronation Hill 7470 528 0.0707 0.001 0.1016 0.004 0.9900 0.045 0.92 948 17 624 26 699 23 26
c29-217u Coronation Hill 10649 710 0.0668 0.000 0.1026 0.004 0.9441 0.032 0.94 830 14 629 23 675 17 19
c29-217r Coronation Hill 3590 264 0.0735 0.001 0.1048 0.004 1.0621 0.040 0.93 1028 18 642 24 735 20 29
c29-217n Coronation Hill 4666 340 0.0729 0.000 0.1107 0.003 1.1129 0.027 0.93 1011 13 677 17 760 13 25
c29-217z Coronation Hill 9177 677 0.0740 0.002 0.1145 0.004 1.1687 0.054 0.83 1042 49 699 23 786 25 25
c29-217w Coronation Hill 5453 412 0.0758 0.001 0.1147 0.005 1.1984 0.055 0.90 1089 31 700 28 800 25 27
c29-217x Coronation Hill 3742 292 0.0782 0.001 0.1177 0.002 1.2695 0.034 0.87 1152 24 717 14 832 15 28
C29-214Aa Coronation Hill 16126 1278 0.0796 0.0011 0.0838 0.004 0.9202 0.061 1.00 1188 27 519 26 662 33 56
C29-214Ac Coronation Hill 34598 2819 0.0814 0.0012 0.1312 0.001 1.4713 0.021 0.97 1230 28 795 6 919 9 35
C29-214Ae Coronation Hill 22206 1803 0.0811 0.0006 0.0652 0.006 0.7297 0.067 1.00 1223 15 407 34 556 39 67
C29-214Af Coronation Hill 4306 294 0.0683 0.0005 0.0180 0.001 0.1690 0.010 0.99 877 14 115 6 159 8 87
C29-214Ag Coronation Hill 17758 1444 0.0805 0.0030 0.1046 0.005 1.1602 0.067 0.76 1209 74 641 32 782 31 47
C29-214Ah Coronation Hill 31182 2460 0.0798 0.0022 0.1103 0.006 1.2132 0.069 0.88 1193 54 674 35 807 32 43
C29-214Al Coronation Hill 18264 1445 0.0793 0.0005 0.0924 0.007 1.0097 0.078 1.00 1179 13 570 44 709 40 52
C29-214c Coronation Hill 12533 1052 0.0839 0.0002 0.0930 0.002 1.0759 0.019 0.26 1291 4 573 10 742 10 56
C29-214d Coronation Hill 21315 1789 0.0840 0.0002 0.0935 0.006 1.0826 0.066 1.00 1291 4 576 34 745 32 55
C29-214e Coronation Hill 22417 1881 0.0839 0.0002 0.0955 0.003 1.1048 0.029 1.00 1290 4 588 15 756 14 54
C29-214f Coronation Hill 59232 4955 0.0837 0.0001 0.0958 0.003 1.1053 0.037 1.00 1285 3 590 19 756 18 54
C29-214g Coronation Hill 20506 1723 0.0840 0.0002 0.0852 0.003 0.9862 0.030 1.00 1292 4 527 16 697 16 59
265

Corrected ratios
Apparent ages ( ±1σ, Ma)**
Sample
Deposit
206 Pb/ 204 Pb
207 Pb/ 204 Pb
207 Pb/ 206 Pb ±2σ
206 Pb/ 238 U ±2σ
207 Pb/ 235 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
C29-214h Coronation Hill 11979 1011 0.0845 0.0002 0.0781 0.003 0.9102 0.039 1.00 1303 5 485 20 657 20 63
C29-214j Coronation Hill 15197 1274 0.0838 0.0001 0.0936 0.004 1.0815 0.042 1.00 1288 3 577 22 744 21 55
C29-295k Coronation Hill 891 58 0.0650 0.004 0.0293 0.01 0.2595 0.06 0.89 774 126 186 50 234 45 76
C29-295l Coronation Hill 855 58 0.0679 0.002 0.0299 0.00 0.2798 0.03 0.86 865 65 190 22 250 26 78
C29-295h Coronation Hill 1330 87 0.0655 0.002 0.0299 0.01 0.2714 0.05 0.93 790 69 190 35 244 41 76
C29-295g Coronation Hill 2587 154 0.0593 0.001 0.0397 0.00 0.3251 0.03 0.91 580 31 251 20 286 22 57
C29-295d Coronation Hill 10794 605 0.0571 0.002 0.0392 0.00 0.3094 0.04 0.92 495 87 248 28 274 34 50
C29-295f Coronation Hill 3370 175 0.0516 0.000 0.0381 0.00 0.2715 0.01 0.91 269 20 241 9 244 9 10
C29-295j Coronation Hill 2906 160 0.0553 0.002 0.0430 0.00 0.3278 0.03 0.91 423 64 272 28 288 27 36
C29-295a Coronation Hill 3104 175 0.0560 0.001 0.0455 0.00 0.3515 0.03 0.92 453 40 287 19 306 20 37
C29-295b Coronation Hill 1217 88 0.0733 0.002 0.0426 0.00 0.4298 0.02 0.72 1021 64 269 13 363 16 74
C29-295c Coronation Hill 7629 409 0.0535 0.000 0.0502 0.00 0.3703 0.03 0.94 349 19 316 22 320 20 10
C29-295i Coronation Hill 5676 331 0.0583 0.001 0.0603 0.01 0.4851 0.07 0.94 540 38 377 49 402 50 30
C29-295e Coronation Hill 8181 560 0.0681 0.002 0.1737 0.02 1.6303 0.22 0.92 871 47 1033 136 982 85 18
C29-217Aa Coronation Hill 2840 214 0.0757 0.002 0.1052 0.004 1.1500 0.05 0.84 1088 45 645 25 777 25 41
C29-217Ad Coronation Hill 1972 155 0.0787 0.001 0.0846 0.003 0.9181 0.03 0.89 1165 26 523 18 661 15 55
C29-217Ae Coronation Hill 3082 229 0.0744 0.001 0.0967 0.003 1.0600 0.04 0.90 1053 27 595 18 734 18 43
C29-217An Coronation Hill 5575 489 0.0876 0.001 0.1202 0.005 1.4525 0.08 0.93 1374 27 732 31 911 32 47
C29-217Ap Coronation Hill 15919 1416 0.0889 0.001 0.1366 0.013 1.6767 0.18 0.90 1402 26 826 76 1000 69 41
C29-217Aq Coronation Hill 7776 653 0.0838 0.001 0.1242 0.012 1.4370 0.15 0.95 1289 23 755 67 904 62 41
C29-217Ar Coronation Hill 3736 259 0.0696 0.001 0.0585 0.005 0.5610 0.04 0.91 916 41 366 28 452 29 60
C29-217At Coronation Hill 4486 361 0.0804 0.001 0.0877 0.008 0.9720 0.09 0.95 1206 19 542 45 689 48 55
C29-217Au Coronation Hill 14240 1190 0.0838 0.002 0.1490 0.007 1.7900 0.07 0.85 1288 39 895 37 1042 24 30
C29-217Ac Coronation Hill 2535 193 0.0761 0.001 0.0924 0.003 0.9695 0.03 0.89 1098 26 570 19 688 15 48
C29-217Ab Coronation Hill 5057 349 0.0692 0.002 0.1011 0.006 0.9649 0.05 0.86 905 49 621 32 686 24 31
C29-217Ag Coronation Hill 3781 265 0.0702 0.001 0.0984 0.005 0.9516 0.04 0.93 934 21 605 28 679 21 35
C29-217Ai Coronation Hill 7467 494 0.0661 0.001 0.0954 0.004 0.8691 0.03 0.93 809 16 587 21 635 16 27
C29-217Aj Coronation Hill 5061 343 0.0678 0.001 0.0942 0.003 0.8807 0.03 0.91 862 21 581 19 641 14 33
C29-217Ak Coronation Hill 5124 350 0.0683 0.001 0.0947 0.004 0.8915 0.03 0.94 879 21 583 26 647 18 34
C29-217Al Coronation Hill 5420 378 0.0698 0.001 0.1059 0.008 1.0196 0.08 0.94 923 16 649 45 714 38 30
C29-217Am Coronation Hill 6716 479 0.0714 0.001 0.1078 0.003 1.0617 0.04 0.86 970 37 660 19 735 21 32
C29-217Ao Coronation Hill 10150 802 0.0789 0.001 0.1244 0.009 1.3530 0.11 0.94 1169 33 756 52 869 47 35
C29-217As Coronation Hill 3916 294 0.0751 0.001 0.1077 0.004 1.1158 0.04 0.93 1072 14 659 21 761 18 39
C29-217Av Coronation Hill 7613 531 0.0698 0.001 0.0991 0.004 0.9535 0.04 0.93 922 22 609 22 680 21 34
C29-217Ax Coronation Hill 6273 441 0.0704 0.001 0.1018 0.005 0.9873 0.05 0.92 939 23 625 29 697 23 33
266

Corrected ratios
Apparent ages ( ±1σ, Ma)**
Sample
Deposit
206 Pb/ 204 Pb
207 Pb/ 204 Pb
207 Pb/ 206 Pb ±2σ
206 Pb/ 238 U ±2σ
207 Pb/ 235 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
Cor29_205B Coronation Hill 4414 402 0.0916 - 0.1682 - 2.1244 - - 1459 39 1002 106 1157 83 -
Cor29_205Ha Coronation Hill 4541 385 0.0848 - 0.0830 - 0.9709 - - 1311 23 514 39 689 39 -
Cor29_205Ia Coronation Hill 1120 103 0.0919 - 0.1014 - 1.2850 - - 1465 25 623 50 839 50 -
Cor29_205Ib Coronation Hill 1183 114 0.0966 - 0.1388 - 1.8489 - - 1560 17 838 33 1063 28 -
Cor29_205I Coronation Hill 1339 123 0.0930 - 0.1283 - 1.6634 - - 1487 52 778 136 995 166 -
Cor29_205Kb Coronation Hill 2253 181 0.0803 - 0.1119 - 1.2385 - - 1204 16 684 31 818 29 -
Cor29_205L Coronation Hill 1248 127 0.1017 - 0.1643 - 2.3097 - - 1655 50 981 95 1215 93 -
Cor29_201.6Ac Coronation Hill 1684 136 0.0807 - 0.1046 - 1.1679 - - 1214 58 641 81 786 89 -
Cor29_205O Coronation Hill 1270 116 0.0913 - 0.1112 - 1.4001 - - 1452 44 678 52 889 53 -
Cor29_201.6Aa Coronation Hill 1096 107 0.0975 - 0.1284 - 1.7258 - - 1577 53 779 59 1018 53 -
Cor29_201.6Ab Coronation Hill 1322 119 0.0902 - 0.1093 - 1.3615 - - 1531 54 668 67 872 73 -
Cor29_201.6Ad Coronation Hill 4108 293 0.0702 - 0.0793 - 0.7687 - - 935 86 492 29 580 44 -
Cor29_201.6Bbc Coronation Hill 1508 127 0.0842 - 0.1182 - 1.3736 - - 1298 35 720 27 878 27 -
Cor29_201.6aa Coronation Hill 1446 125 0.0864 - 0.0959 - 1.1432 - - 1348 16 790 13 774 12 -
Cor29_201.6abc Coronation Hill 1234 112 0.0911 - 0.1089 - 1.3692 - - 1449 33 666 44 876 48 -
Cor29_201.6D Coronation Hill 1086 114 0.1053 - 0.1967 - 2.8569 - - 1719 31 1157 44 1371 43 -
Cor29_201.6Ga Coronation Hill 2825 214 0.0756 - 0.1012 - 1.0564 - - 1085 36 622 52 732 53 -
Cor29_201.6Gb Coronation Hill 2121 171 0.0808 - 0.1180 - 1.3147 - - 1216 26 719 60 842 54 -
El Sherana 1a El Sherana - - 0.0924 - 0.0564 - 0.8206 - - 1500 - 354 - 610 - -
El Sherana 1b El Sherana - - 0.0935 - 0.0650 - 0.8695 - - 1498 - 406 - 636 - -
El Sherana 1c El Sherana - - 0.0987 - 0.0675 - 0.9866 - - 1600 - 421 - 698 - -
El Sherana 2a El Sherana - - 0.0999 - 0.0700 - 1.0588 - - 1625 - 436 - 756 - -
El Sherana 2b El Sherana - - 0.0768 - 0.0571 - 0.6513 - - 1116 - 358 - 510 - -
El Sherana 3b El Sherana - - 0.1105 - 0.0626 - 1.1142 - - 1810 - 392 - 762 - -
El Sherana 4a El Sherana - - 0.0907 - 0.0622 - 0.9018 - - 1441 - 388 - 654 - -
El Sherana 4b El Sherana - - 0.0793 - 0.0560 - 0.7712 - - 1180 - 352 - 582 - -
El Sherana 4c El Sherana - - 0.1024 - 0.0826 - 1.4012 - - 1665 - 512 - 890 - -
El Sherana 5c El Sherana - - 0.0938 - 0.2121 - 3.1739 - - 1505 - 1240 - 1452 - -
El Sherana 5d El Sherana - - 0.0883 - 0.0585 - 0.8515 - - 1388 - 366 - 626 - -
El Sherana 6b El Sherana - - 0.1010 - 0.0631 - 0.9921 - - 1640 - 395 - 700 - -
El Sherana 7a El Sherana - - 0.0942 - 0.0728 - 1.0060 - - 1515 - 452 - 708 - -
El Sherana 7b El Sherana - - 0.0892 - 0.0655 - 0.8338 - - 1408 - 409 - 616 - -
El Sherana 2 El Sherana 1739 - 0.0916 0.0031 0.0705 0.0033 0.8054 0.0167 0.176 1460 62 439 20 600 9 70
El Sherana 3 El Sherana 1439 - 0.0946 0.0032 0.0724 0.0038 0.8861 0.0181 0.103 1520 63 451 23 644 10 70
El Sherana 4 El Sherana 1356 - 0.0959 0.0034 0.0747 0.0030 0.9551 0.0183 0.114 1545 66 464 18 681 9 70
267

Corrected ratios
Apparent ages ( ±1σ, Ma)**
Sample
Deposit
206 Pb/ 204 Pb
207 Pb/ 204 Pb
207 Pb/ 206 Pb ±2σ
206 Pb/ 238 U ±2σ
207 Pb/ 235 U ±2σ R‡
207 Pb/ 206 Pb ±
206 Pb/ 238 U ±
207 Pb/ 235 U ± Disc‡
El Sherana 5 El Sherana 3605 - 0.0780 0.0023 0.0591 0.0021 0.6221 0.0110 0.134 1146 58 370 13 491 7 68
El Sherana 7 El Sherana 1767 - 0.0935 0.0041 0.0706 0.0040 0.8149 0.0195 0.020 1498 80 440 24 605 11 71
El Sherana 8 El Sherana 3975 - 0.0885 0.0043 0.0656 0.0043 0.7161 0.0155 0.230 1394 90 410 26 548 9 71
El Sherana 9 El Sherana 1251 - 0.0989 0.0048 0.0893 0.0078 1.1072 0.0697 0.632 1604 87 551 46 757 33 66
El Sherana 11 El Sherana 1944 - 0.1099 0.0068 0.0715 0.0052 0.7964 0.0207 0.035 1798 109 445 31 595 12 75
El Sherana 12 El Sherana 1526 - 0.1116 0.0057 0.0754 0.0054 0.9074 0.0193 0.033 1825 90 469 32 656 10 74
El Sherana 13 El Sherana 1476 - 0.0884 0.0022 0.0735 0.0021 0.8950 0.0135 0.204 1392 48 457 12 649 7 67
El Sherana 14 El Sherana 1707 - 0.0843 0.0022 0.0657 0.0018 0.7582 0.0109 0.026 1300 50 410 11 573 6 68
El Sherana 17 El Sherana 1087 - 0.0882 0.0015 0.0934 0.0044 1.1724 0.0593 0.924 1387 33 575 26 788 27 59
El Sherana 18 El Sherana 1257 - 0.0920 0.0015 0.1394 0.0114 1.7701 0.1447 0.941 1467 32 841 64 1035 52 43
El Sherana 19 El Sherana 1388 - 0.0886 0.0020 0.0808 0.0045 0.9891 0.0550 0.897 1395 42 501 27 698 28 64
268

APPENDIX H
Electron microprobe data and temperatures of various chlorite phases from deposits
of the South Alligator River area
Sample ID. Al 2O 3 CaO FeO K2O MgO MnO Na 2O SiO 2 TiO 2 Cl F Temp ( o )
C29-217A-1 18.65 0.03 15.85 0.03 21.74 0.15 0.03 29.64 0.01 0.03 0.35 258
C29-217A-2 18.79 0.05 15.68 0.00 22.59 0.13 0.05 29.48 0.02 0.02 0.26 271
C29-217A-3 18.73 0.02 15.61 0.01 22.58 0.15 0.04 29.62 0.01 0.03 0.26 267
C29-217A-4 18.85 0.05 15.23 0.02 22.26 0.15 0.00 30.21 0.00 0.03 0.14 252
C29-217A-5 18.45 0.06 16.03 0.02 21.79 0.12 0.00 29.33 0.00 0.03 0.18 263
C29-217A-6 19.26 0.06 14.05 0.08 21.52 0.15 0.04 31.08 0.02 0.04 0.59 227
C29-217A-7 19.31 0.01 14.09 0.04 22.85 0.14 0.04 29.95 0.00 0.03 0.17 262
C29-217A-8 19.03 0.05 16.66 0.02 20.88 0.11 0.00 29.37 0.01 0.03 0.15 263
C29-217A-11 18.83 0.04 14.44 0.01 21.67 0.12 0.03 29.86 0.00 0.05 0.26 247
C29-217A-12 19.06 0.10 14.01 0.17 20.48 0.08 0.04 30.59 0.00 0.06 0.34 258
C29-217A-13 18.42 0.04 15.19 0.03 21.94 0.16 0.02 29.19 0.00 0.03 0.40 262
C29-217A-14 19.11 0.02 16.48 0.01 21.28 0.19 0.05 29.70 0.00 0.02 0.52 262
C29-217A-15 18.20 0.05 14.73 0.00 21.15 0.13 0.00 28.51 0.00 0.05 0.36 261
C29-217A-16 19.07 0.05 15.05 0.00 22.23 0.07 0.00 29.61 0.00 0.04 0.25 264
c29217a-27 20.84 0.09 3.28 0.18 26.41 0.04 0.03 32.89 0.02 0.08 0.31 203
c29217a-25 20.69 0.09 3.46 0.16 25.68 0.01 0.02 33.08 0.04 0.07 0.39 191
c29217a-24 20.06 0.09 3.43 0.20 26.21 0.04 0.05 33.06 0.03 0.06 0.35 190
C29-217B-6 23.98 0.15 7.16 0.28 18.47 0.08 0.07 32.62 0.01 0.03 0.06 187
c29217a-21 20.39 0.11 3.83 0.32 25.25 0.02 0.03 33.10 0.01 0.05 0.23 186
C29-217B-15 22.15 0.22 8.63 0.15 18.95 0.13 0.03 32.26 0.00 0.02 0.21 184
c29217a-29 20.42 0.08 3.21 0.27 25.31 0.02 0.06 33.23 0.00 0.06 0.45 180
C29-217B-7 23.86 0.15 8.51 0.48 17.50 0.14 0.09 33.03 0.00 0.03 0.21 178
c29217a-28 20.40 0.09 3.45 0.18 25.08 0.03 0.01 33.33 0.01 0.06 0.46 177
C29-217B-5 24.52 0.15 6.59 0.31 17.57 0.08 0.10 33.14 0.00 0.05 0.18 173
C29-214B-30 19.84 0.04 19.72 0.03 18.91 0.15 0.01 28.91 0.02 0.01 0.21 170
C29-214B-50 19.25 0.05 16.08 0.05 20.68 0.12 0.04 29.00 0.00 0.02 0.50 167
c29217a-31 20.21 0.12 3.83 0.37 24.89 0.03 0.05 33.91 0.00 0.06 0.40 166
C29-217B-16 22.51 0.18 8.14 0.16 18.55 0.08 0.07 33.22 0.04 0.04 0.29 165
C29-217B-13 21.30 5.87 5.82 0.78 14.38 0.31 0.01 31.62 0.01 0.03 0.05 164
C29-214B-41 20.03 0.06 16.75 0.03 20.70 0.13 0.00 29.10 0.03 0.01 0.46 163
C29-217B-2 25.05 0.16 6.91 0.49 16.01 0.07 0.08 33.33 0.00 0.04 0.00 162
C29-217B-4 22.87 0.17 7.06 0.24 18.15 0.11 0.05 33.03 0.01 0.04 0.07 162
C29-214B-40 19.27 0.03 17.64 0.00 20.68 0.14 0.03 29.19 0.02 0.02 0.37 160
c29217a-22 20.81 0.11 3.71 0.52 23.73 0.00 0.04 34.34 0.02 0.05 0.49 154
c29217a-23 20.77 0.12 3.75 0.63 23.34 0.05 0.07 34.34 0.02 0.05 0.43 150
C29-214B-6 21.06 0.05 13.86 0.02 20.66 0.11 0.00 29.48 0.01 0.00 0.45 150
C29-214B-42 20.16 0.02 17.24 0.02 20.59 0.14 0.03 29.46 0.00 0.01 0.34 150
C29-214B-5 20.27 0.08 14.55 0.01 22.21 0.18 0.01 29.75 0.02 0.02 0.44 140
C29-217B-1 24.45 0.18 6.74 0.48 16.59 0.11 0.03 34.52 0.00 0.05 0.12 139
c29217a-17 19.45 0.10 5.15 0.58 23.36 0.09 0.01 34.63 0.01 0.05 0.05 137
c29217a-26 19.62 0.13 4.19 0.41 23.26 0.09 0.04 34.30 0.00 0.05 0.26 137
C29-214B-48 19.89 0.04 15.59 0.05 21.51 0.14 0.02 30.05 0.00 0.02 0.45 129
C29-214B-11 24.61 0.10 2.82 0.13 21.40 0.00 0.04 30.22 0.01 0.12 0.46 123
C29-214B-45 20.22 0.03 13.82 0.02 21.54 0.09 0.02 30.29 0.03 0.02 0.46 120
C29-214B-34 22.62 0.11 11.91 0.12 18.25 0.08 0.00 30.31 0.02 0.03 0.41 119
c29217a-30 20.73 0.12 3.31 0.63 22.33 0.05 0.06 35.47 0.00 0.06 0.34 117
269

Sample ID. Al 2O 3 CaO FeO K2O MgO MnO Na 2O SiO 2 TiO 2 Cl F Temp ( o )
c29217a-19 19.20 0.16 4.00 0.34 23.17 0.06 0.07 35.06 0.01 0.05 0.46 116
c29217a-20 20.14 0.12 4.36 0.38 25.23 0.02 0.00 33.39 0.00 0.06 0.26 116
C29-214B-36 20.21 0.04 14.01 0.03 23.34 0.13 0.03 30.46 0.01 0.01 0.37 114
c29217a-32 18.81 0.16 5.04 0.81 22.33 0.07 0.05 34.92 0.02 0.05 0.23 112
C29-214B-51 20.09 0.10 9.04 0.03 25.20 0.02 0.03 30.53 0.00 0.03 0.57 111
C29-214B-19 23.93 0.10 4.44 0.10 23.79 0.01 0.01 30.58 0.00 0.03 0.37 110
C29-217B-14 24.50 0.17 5.55 0.95 15.79 0.34 0.04 35.63 0.00 0.04 0.12 109
C29-214B-25 21.13 0.08 10.77 0.03 23.90 0.03 0.00 30.64 0.00 0.04 0.44 107
C29-217B-8 22.91 0.21 5.73 0.76 17.22 0.33 0.08 35.53 0.01 0.03 0.07 106
C29-214B-21 23.38 0.09 6.70 0.04 24.40 0.07 0.04 30.73 0.03 0.01 0.64 104
C29-217B-25 22.05 0.23 8.09 0.74 16.11 0.13 0.04 35.16 0.02 0.04 0.38 101
C29-214B-32 23.83 0.04 4.15 0.04 27.15 0.00 0.00 30.81 0.02 0.01 0.50 101
C29-214B-23 22.36 0.08 9.39 0.06 23.07 0.14 0.05 30.85 0.02 0.02 0.30 100
C29-214B-33 23.93 0.11 3.35 0.03 26.38 0.01 0.01 30.84 0.01 0.02 0.29 100
C29-217B-29 21.78 0.24 7.02 0.91 17.38 0.20 0.05 35.65 0.01 0.03 0.27 99
C29-217B-10 23.73 0.20 6.10 0.47 17.93 0.40 0.03 37.36 0.02 0.03 0.13 98
C29-214B-17 22.15 0.09 11.85 0.05 22.40 0.13 0.03 31.15 0.03 0.02 0.33 89
C29-214B-2 24.44 0.05 3.11 0.06 25.97 0.02 0.03 31.21 0.00 0.02 0.42 86
C29-214B-31 22.61 0.11 8.33 0.04 22.93 0.05 0.02 31.23 0.01 0.03 0.31 86
C29-214B-3 22.38 0.05 11.05 0.07 20.89 0.11 0.04 31.26 0.01 0.03 0.46 85
C29-214B-4 22.25 0.03 9.86 0.03 21.41 0.06 0.04 31.26 0.03 0.01 0.35 85
C29-214B-38 24.82 0.08 5.67 0.03 24.72 0.01 0.03 31.24 0.03 0.02 0.51 85
C29-214B-1 25.09 0.04 4.93 0.03 24.21 0.03 0.02 31.32 0.00 0.02 0.38 82
C29-214B-18 22.83 0.09 8.82 0.06 23.27 0.08 0.01 31.33 0.05 0.04 0.26 82
C29-214B-22 23.20 0.09 8.19 0.04 25.12 0.06 0.01 31.34 0.01 0.01 0.48 82
C29-214B-26 21.69 0.13 9.97 0.16 21.85 0.09 0.06 31.34 0.00 0.03 0.40 82
C29-217B-20 22.04 0.21 6.21 0.75 16.28 0.09 0.07 35.82 0.00 0.03 0.17 80
C29-214B-46 22.80 0.10 11.25 0.03 19.49 0.07 0.03 31.45 0.01 0.02 0.56 78
C29-214B-9 21.68 0.08 10.18 0.06 23.07 0.13 0.00 31.53 0.00 0.02 0.50 75
C29-214B-7 25.18 0.07 4.17 0.07 24.13 0.06 0.02 31.55 0.01 0.02 0.47 74
C29-214B-44 20.95 0.10 9.54 0.06 23.94 0.04 0.04 31.55 0.00 0.02 0.75 74
C29-214B-12 25.44 0.08 6.46 0.09 22.83 0.02 0.00 31.63 0.04 0.04 0.30 71
C29-214B-20 24.22 0.12 4.61 0.07 23.57 0.02 0.00 31.64 0.00 0.02 0.29 71
C29-214B-27 24.97 0.06 7.96 0.10 20.13 0.07 0.01 31.66 0.06 0.02 0.26 70
C29-214B-39 25.02 0.09 5.92 0.03 25.13 0.02 0.00 31.73 0.00 0.02 0.43 68
C29-214B-29 22.24 0.12 10.06 0.03 21.59 0.03 0.05 31.87 0.01 0.05 0.32 62
C29-217B-22 20.91 0.23 7.36 0.94 16.19 0.12 0.04 36.74 0.03 0.04 0.25 57
C29-214B-35 25.48 0.05 6.75 0.12 21.31 0.04 0.02 32.02 0.03 0.03 0.51 57
C29-214B-8 23.16 0.11 11.76 0.04 21.13 0.06 0.06 32.04 0.00 0.04 0.42 56
C29-214B-43 22.98 0.10 8.96 0.03 20.63 0.05 0.04 32.13 0.01 0.03 0.46 53
C29-214B-37 23.44 0.05 9.69 0.09 21.31 0.06 0.01 32.16 0.03 0.03 0.24 52
C29-214B-15 24.29 0.08 8.58 0.10 20.62 0.07 0.01 32.18 0.02 0.04 0.45 51
C29-214B-14 20.99 0.14 5.85 0.46 23.58 0.07 0.07 32.23 0.02 0.06 0.30 49
C29-214B-28 25.71 0.03 3.48 0.06 23.72 0.02 0.00 32.29 0.02 0.03 0.34 47
C29-214B-10 25.77 0.14 2.59 0.13 22.97 0.00 0.00 32.34 0.01 0.03 0.31 45
C29-214B-13 24.98 0.12 5.71 0.08 21.56 0.03 0.06 32.35 0.05 0.04 0.48 45
C29-214B-16 25.30 0.10 3.59 0.09 23.35 0.04 0.02 32.35 0.01 0.04 0.41 45
C29-214B-24 21.06 0.19 6.42 0.30 24.07 0.07 0.05 32.96 0.01 0.04 0.75 23
C29-217B-18 21.80 0.25 8.38 0.13 19.64 0.17 0.05 32.34 0.00 0.02 0.14
E32-45B-46 19.68 0.03 33.71 0.01 9.27 0.01 0.04 27.53 0.01 0.01 0.24 285
E32-45B-8 18.31 0.03 32.97 0.02 10.13 0.01 0.01 26.81 0.01 0.00 0.19 287
E32-45B-23 18.49 0.02 34.32 0.06 9.31 0.00 0.02 26.92 0.04 0.01 0.13 287
270

Sample ID. Al 2O 3 CaO FeO K2O MgO MnO Na 2O SiO 2 TiO 2 Cl F Temp ( o )
E32-45B-41 18.48 0.02 36.09 0.03 7.92 0.05 0.01 26.69 0.01 0.01 0.19 287
E32-45B-1 17.66 0.01 33.53 0.02 10.46 0.00 0.00 26.66 0.00 0.00 0.20 288
E32-45B-10 18.31 0.02 32.89 0.02 10.14 0.00 0.01 26.72 0.01 0.00 0.07 288
E32-45B-15 17.94 0.05 33.69 0.02 8.63 0.00 0.00 25.75 0.00 0.00 0.05 292
E32-45B-40 18.01 0.02 33.95 0.00 10.26 0.03 0.04 26.70 0.00 0.00 0.15 292
E32-45B-45 18.70 0.02 34.82 0.01 8.10 0.00 0.02 26.27 0.01 0.01 0.06 292
E32-45B-20 18.61 0.05 34.33 0.06 9.10 0.01 0.00 26.50 0.00 0.01 0.02 294
E32-45B-12 18.83 0.01 32.34 0.01 10.30 0.00 0.01 26.59 0.00 0.00 0.04 296
E32-45B-21 18.06 0.02 33.84 0.03 9.81 0.02 0.02 26.14 0.02 0.01 0.19 299
E32-45B-51 18.14 0.04 35.90 0.00 8.45 0.01 0.00 26.03 0.01 0.01 0.00 300
E32-45B-47 18.62 0.04 36.62 0.02 7.47 0.03 0.01 25.94 0.03 0.02 0.00 302
E32-45B-44 18.27 0.02 34.38 0.01 9.41 0.06 0.00 26.06 0.06 0.00 0.18 303
E32-45B-48 17.87 0.03 34.18 0.05 10.09 0.00 0.00 26.07 0.01 0.01 0.25 303
E32-45B-42 18.79 0.00 34.08 0.02 9.74 0.00 0.01 26.29 0.00 0.01 0.08 306
E32-45B-43 19.16 0.00 33.31 0.01 8.95 0.02 0.06 25.91 0.01 0.01 0.16 306
E32-45B-38 19.19 0.01 35.64 0.02 8.54 0.01 0.00 26.23 0.02 0.00 0.15 309
E32-45B-37 18.74 0.00 33.30 0.00 9.75 0.00 0.00 25.68 0.01 0.01 0.10 313
E32-45B-49 17.97 0.00 36.58 0.03 8.64 0.00 0.02 25.61 0.01 0.01 0.07 313
E32-45B-19 16.96 0.04 35.29 0.05 9.59 0.02 0.00 24.93 0.03 0.01 0.11 318
E32-45B-6 18.62 0.02 34.77 0.00 8.92 0.00 0.00 25.14 0.03 0.01 0.00 323
E32-45B-50 17.41 0.03 35.75 0.00 8.94 0.01 0.02 24.67 0.00 0.01 0.00 324
E32-41B-13 16.52 0.03 34.75 0.08 8.83 0.05 0.02 27.40 0.00 0.05 0.19 226
E32-41B-42 16.89 0.05 35.98 0.03 8.84 0.01 0.00 27.18 0.03 0.03 0.15 234
E32-41B-41 16.22 0.03 34.91 0.08 9.52 0.02 0.02 27.07 0.00 0.08 0.13 237
E32-41B-25 18.82 0.04 36.50 0.05 7.57 0.00 0.00 27.07 0.02 0.01 0.00 238
E32-41B-34 16.71 0.10 36.00 0.04 9.11 0.02 0.06 27.02 0.03 0.05 0.28 239
E32-41B-44 16.26 0.02 34.18 0.05 10.01 0.00 0.09 27.03 0.03 0.06 0.04 239
E32-41B-14 16.72 0.06 35.18 0.03 9.10 0.03 0.08 27.00 0.04 0.04 0.30 240
E32-41B-17 16.32 0.05 35.27 0.04 9.54 0.00 0.00 27.00 0.03 0.03 0.01 240
E32-41B-10 15.80 0.11 33.35 0.05 8.13 0.00 0.10 26.50 0.02 0.04 0.57 240
E32-41B-37 16.93 0.02 35.20 0.02 9.47 0.01 0.03 26.82 0.01 0.03 0.14 247
E32-41B-26 19.30 0.00 34.52 0.04 9.41 0.01 0.06 26.80 0.02 0.01 0.18 247
E32-41B-5 16.20 0.05 35.29 0.01 8.57 0.00 0.00 27.21 0.04 0.05 0.19 248
E32-41B 16.27 0.03 35.12 0.01 9.60 0.00 0.04 27.73 0.00 0.02 0.22 249
E32-41B-19 17.49 0.00 34.08 0.02 9.64 0.00 0.03 26.75 0.03 0.02 0.03 249
E32-41B-16 16.26 0.03 34.79 0.03 9.41 0.00 0.04 26.75 0.03 0.04 0.27 249
E32-41B-12 16.39 0.02 34.82 0.07 9.36 0.03 0.04 26.72 0.00 0.03 0.05 250
E32-41B-15 17.76 0.04 33.84 0.04 9.46 0.01 0.07 26.60 0.02 0.03 0.12 255
E32-41B-43 17.13 0.01 34.63 0.03 9.17 0.03 0.05 26.55 0.00 0.08 0.05 256
E32-41B-28 19.50 0.02 34.30 0.08 9.20 0.00 0.01 26.57 0.04 0.01 0.12 256
E32-41B-18 16.90 0.00 33.96 0.03 9.79 0.01 0.04 26.51 0.01 0.02 0.27 258
E32-41B-39 16.05 0.04 35.06 0.07 9.39 0.00 0.05 26.35 0.06 0.03 0.33 264
E32-41B-3 16.96 0.04 35.19 0.02 9.23 0.00 0.01 27.10 0.03 0.02 0.18 267
E32-41B-7 16.84 0.04 35.25 0.02 8.97 0.01 0.01 26.83 0.02 0.03 0.20 268
E32-41B-1 16.75 0.03 35.11 0.02 8.69 0.00 0.00 26.49 0.00 0.02 0.10 270
E32-41B-2 17.33 0.00 34.93 0.00 9.20 0.00 0.02 26.95 0.03 0.02 0.04 273
E32-41B-8 17.21 0.00 34.82 0.00 8.62 0.02 0.03 26.50 0.01 0.02 0.04 273
E32-41B-35 19.32 0.02 32.91 0.07 9.85 0.01 0.07 26.10 0.03 0.07 0.27 273
E32-45B-27 15.69 0.02 27.03 0.04 15.25 0.01 0.03 28.64 0.00 0.02 0.22 236
E32-41B 16.27 0.03 35.12 0.01 9.60 0.00 0.04 27.73 0.00 0.02 0.22 249
E32-45B-26 17.28 0.01 31.92 0.07 11.25 0.06 0.00 28.01 0.01 0.00 0.15 255
E32-45B-13 16.51 0.03 32.13 0.01 10.34 0.00 0.00 26.79 0.05 0.06 0.05 261
271

Sample ID. Al 2O 3 CaO FeO K2O MgO MnO Na 2O SiO 2 TiO 2 Cl F Temp ( o )
E32-45B-3 16.55 0.01 32.39 0.01 10.83 0.06 0.00 27.03 0.01 0.01 0.20 263
E32-45B-30 17.12 0.01 33.93 0.01 10.28 0.01 0.01 27.49 0.00 0.01 0.07 265
E32-45B-7 16.91 0.01 32.73 0.00 11.20 0.00 0.03 27.44 0.02 0.00 0.11 266
E32-45B-5 16.17 0.00 36.08 0.02 9.32 0.00 0.00 26.90 0.05 0.00 0.20 267
E32-45B-4 15.76 0.01 33.41 0.03 10.77 0.00 0.00 26.47 0.04 0.00 0.11 270
E32-45B-11 17.46 0.05 31.79 0.01 11.66 0.01 0.00 27.59 0.01 0.01 0.27 270
E32-45B-24 16.71 0.01 33.86 0.01 10.11 0.06 0.03 26.89 0.01 0.01 0.00 270
E32-45B-32 17.45 0.02 29.84 0.05 12.83 0.00 0.00 27.59 0.01 0.02 0.28 270
E32-41B-1 16.75 0.03 35.11 0.02 8.69 0.00 0.00 26.49 0.00 0.02 0.10 270
E32-45B-25 17.54 0.05 30.62 0.02 12.91 0.00 0.00 27.88 0.00 0.02 0.33 271
E32-45B-2 17.09 0.02 32.87 0.03 11.04 0.01 0.01 27.15 0.02 0.01 0.16 273
E32-41B-2 17.33 0.00 34.93 0.00 9.20 0.00 0.02 26.95 0.03 0.02 0.04 273
E32-45B-17 17.51 0.03 32.68 0.04 10.86 0.03 0.00 27.18 0.00 0.00 0.06 274
E32-45B-9 17.75 0.03 33.68 0.01 10.19 0.00 0.00 27.24 0.00 0.00 0.07 275
E32-41A-15 16.31 0.05 31.92 0.03 11.53 0.00 0.00 27.55 0.00 0.05 0.16 220
E32-41A-22 16.31 0.05 36.41 0.02 9.52 0.02 0.07 27.53 0.02 0.02 0.08 221
E32-41A-33 16.42 0.02 32.82 0.01 11.37 0.00 0.01 27.51 0.00 0.01 0.00 222
E32-41A-29 16.77 0.00 33.43 0.01 10.71 0.05 0.03 27.45 0.00 0.01 0.08 224
E32-41A-3 16.37 0.02 36.20 0.01 9.06 0.01 0.00 27.44 0.01 0.01 0.06 224
E32-41A-21 16.17 0.09 35.82 0.02 9.22 0.03 0.03 27.43 0.00 0.04 0.02 225
E32-41A-37 17.52 0.03 31.73 0.00 12.00 0.02 0.01 27.38 0.01 0.03 0.18 226
E32-41A-23 16.39 0.05 36.20 0.02 9.78 0.00 0.02 27.39 0.01 0.03 0.32 226
E32-41A-42 17.50 0.03 32.09 0.01 11.88 0.00 0.06 27.36 0.03 0.02 0.30 227
E32-41A-41 17.00 0.02 31.84 0.00 11.59 0.00 0.04 27.31 0.03 0.01 0.23 229
E32-41A-24 16.28 0.02 35.08 0.00 9.76 0.00 0.00 27.29 0.02 0.00 0.21 230
E32-41A-10 16.95 0.02 32.66 0.02 11.11 0.00 0.04 27.26 0.01 0.06 0.18 231
E32-41A-26 16.36 0.02 36.61 0.02 8.87 0.03 0.00 27.25 0.01 0.02 0.04 231
E32-41A-30 16.87 0.06 31.45 0.01 11.75 0.00 0.02 27.12 0.01 0.03 0.07 236
E32-41A-38 16.65 0.05 35.16 0.01 9.33 0.00 0.00 27.12 0.02 0.02 0.23 236
E32-41A-14 16.79 0.03 35.31 0.02 9.38 0.00 0.03 27.11 0.00 0.02 0.15 236
E32-41A-43 16.85 0.05 35.53 0.00 9.08 0.02 0.00 27.03 0.02 0.00 0.00 239
E32-41A-57 16.51 0.02 36.01 0.00 9.09 0.02 0.02 27.00 0.03 0.00 0.00 240
E32-41A-25 16.43 0.01 35.58 0.01 9.45 0.02 0.03 27.01 0.03 0.02 0.23 240
E32-41A-19 16.95 0.00 35.96 0.00 9.15 0.00 0.03 26.98 0.03 0.01 0.10 241
E32-41A-16 17.61 0.00 33.30 0.01 10.05 0.00 0.00 26.96 0.03 0.02 0.00 242
E32-41A-20 16.63 0.02 35.59 0.00 9.48 0.03 0.00 26.89 0.02 0.01 0.10 244
E32-41A-27 17.14 0.00 35.84 0.01 9.15 0.05 0.00 26.71 0.05 0.01 0.13 251
E32-41A-53 16.69 0.02 35.95 0.01 8.92 0.04 0.03 26.67 0.02 0.01 0.14 252
E32-41A-4 18.09 0.02 35.25 0.00 8.42 0.04 0.03 26.57 0.03 0.01 0.00 256
E32-41A-56 17.51 0.01 35.76 0.00 8.82 0.00 0.00 26.52 0.07 0.01 0.14 258
E32-41A-59 19.54 0.05 34.45 0.03 8.77 0.01 0.02 26.19 0.02 0.01 0.50 270
E32-41A-54 16.02 0.08 34.84 0.01 8.64 0.00 0.00 26.13 0.01 0.02 0.22 272
E32-41A-58 19.55 0.06 33.64 0.03 9.14 0.03 0.06 26.00 0.01 0.01 0.17 277
E32-41A-52 19.61 0.02 34.76 0.01 8.14 0.02 0.00 25.95 0.00 0.01 0.11 278
272

APPENDIX I
Structural measurements (strike and dip) and stereoplot of different structures from
the Cinch Lake deposit
Mafic dykes
Strike ( o ) Dip ( o )
320 80
240 80
240 85
245 80
245 85
320 85
Mineralized veins
Strike ( o ) Dip ( o )
125 75
320 78
110 80
130 85
35 90
335 85
215 70
20 60
10 60
15 80
15 85
65 80
225 55
280 90
285 90
270 90
320 75
270 80
300 85
310 90
350 85
280 75
340 90
310 75
320 90
270 85
260 90
305 80
290 85
280 90
270 90
310 90
305 80
315 90
310 90
318 90
315 90
320 90
310 90
310 90
317 85
316 90
305 90
270 90
290 80
280 55
270 60
272 60
280 90
280 70
300 85
270 80
280 70
278 75
220 60
320 90
300 90
305 85
Foliation
Strike ( o ) Dip ( o )
245 40
235 50
240 55
245 75
250 60
240 80
240 80
240 80
245 75
295 60
290 35
250 85
Joints
Strike ( o ) Dip ( o )
315 80
325 75
345 75
265 80
235 80
15 82
295 75
315 80
255 90
245 30
275 80
45 30
20 30
0 70
80 85
310 85
125 80
240 75
110 75
285 60
285 60
290 70
290 75
0 70
65 75
160 75
125 50
245 75
295 60
290 35
350 60
350 60
70 80
290 80
10 80
230 90
10 75
230 90
10 75
245 80
200 80
60 90
273

250 85
330 40
145 70
25 65
30 30
270 90
290 60
280 55
270 60
272 60
280 90
280 70
300 85
270 80
270 80
280 70
278 75
220 60
320 90
300 90
305 75
300 80
325 70
175 85
295 70
105 85
285 69
315 65
310 70
305 70
305 85
395 80
250 80
305 75
250 75
210 80
310 70
350 45
305 75
300 70
240 85
105 60
215 60
165 85
150 60
125 65
110 65
110 55
100 85
135 85
40 65
85 66
320 70
240 80
105 60
220 45
Quartz veins
Strike ( o ) Dip ( o )
230 50
240 50
240 70
240 40
235 70
250 60
274

Foliations
Mafic dykes
275

Mineralized veins
Quartz veins
276

Shear zone
Joints
277