StratigraphJc, Diagenetic and Geochemical Study of Cretaceous Strata in
Central Saskatchewan
A thesis
Submitted to the Faculty of Graduate Studies and Research
In Partial Fulfillment of the Requirements
For the Degree of
Master of Science
In Geology
University of Regina
by
Autumn Q Wang
Regina, Saskatchewan
August, 2010
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••I Canada UNIVERSITY OF REGINA
FACULTY OF GRADUATE STUDIES AND RESEARCH
SUPERVISORY AND EXAMINING COMMITTEE
Qiuxia (Autumn) Wang, candidate for the degree of Master of Science in Geology, has presented a thesis titled, Stratigraphic, Diagenetic and Geochemical Study of Cretaceous Strata in Central Saskatchewan, in an oral examination held on May 7, 2010. The following committee members have found the thesis acceptable in form and content, and that the candidate demonstrated satisfactory knowledge of the subject material.
External Examiner: Ms. Melinda Yurowski, Subsurface Geological Lab
Co-Supervisor: Dr. Guoxiang Chi, Department of Geology
Co-Supervisor: *Dr. Per Kent Pedersen, Adjunct Professor, Department of Geology
Committee Member: Dr. Hairuo Qing, Department of Geology
Chair of Defense: Dr. Xue Dong Yang, Department of Computer Science
*Not present at defense Abstract
The poorly studied Cretaceous succession in central Saskatchewan is examined for vertical changes in sedimentary facies and diagenetic features in two continuous cores (3-28-33-23W2 and 6-18-36-6W3) in this study. The studied area includes Townships 28 to 41, Ranges 10 to 1 West of the Third
Meridian and Ranges 28 to 20 West of the Second Meridian. Two hundred and four samples were collected and analyzed.
Facies analysis shows that the Cretaceous was deposited in marginal marine to marine environments with facies changes closely related to sea-level variations. Four uncomformities were identified through core logging in between the Jurassic Success Formation and the Cantuar Formation, Cantuar and Pense
Formations, the Second White Specks and First White Specks, and the Milk
River and Lea Park Formations.
A stratigraphic framework based on cores and well log correlations from southwestern Saskatchewan to southeastern Saskatchewan places the studied sections in a regional stratigraphic context. The regional cross section shows an eastern thinning trend over the Colorado Group, and indicates that the high topographic relief of the Cantuar Formation was scoured by Pense and Joli Fou transgression.
The composition of the studied sandstones varies from quartzarenite, sublitharenite, subarkose, and litharenite to feldspathic litharenite. The diagenetic study of sandstones indicates that cementation, compaction, dissolution and
I replacement were the main diagenetic processes. The porosity, estimated from point counting (n=200), ranges from 0% to 46%, and was mostly between 1% and 25%.
The carbon and oxygen isotope analysis of calcite cements indicates that the significant depletion of 5180 values relates to the influence of meteoric water.
The depleted 513C values may have been caused by meteoric water influx that
13 brought in low 5 C carbon isotope composition from soil-derived C02 or by the anaerobic microbial oxidation of organic carbon.
The TOC analysis indicates that most of the shale of the Colorado Group in central Saskatchewan has a good to excellent source-rock potential. The organic matter of the Second White Specks and Carlile shale consists of a mixture of Type II and Type III kerogen, which is oil/gas prone. All of the other shales fall into the gas prone field, with mainly type III organic matter. The Tmax data and Ro value (<0.4%) indicates that the source rocks in central
Saskatchewan are immature. These rocks are above the thermogenic oil and gas windows and gas production may be limited to bacterially-generated biogenic methane.
II Acknowledgements
This thesis is supported by an NSERC -CDR grant from Profico Energy and a Saskatchewan Industry and Resources grant to Drs. Guoxiang Chi and
Per Kent Pedersen.
I would like to thank my supervisors Dr. Guoxiang Chi and Dr. Per Kent
Pedersen for their strong support, invaluable discussion, patience and encouragement.
Particular thanks are due to Drs. J.E.Christopher and D.M. Kent for help in core logging and for stimulating discussions. Gratitude is also expressed to the staff of the Subsurface Geological Laboratory, and Saskatchewan Energy and
Resources, for logistical support for core logging.
A special thanks to my husband Jilu who always gives me encouragement, support and love.
I extend my thanks to my colleague Michelle Hawke for support and assistance in the preparation of my thesis.
Ill Table of Contents
Abstract I
Acknowledgements III
Table of Contents IV
List of Table VU
List of figures VM
Chapter 1 Introduction 1
1.1 Study area 1
1.2 General stratigraphy 3
1.3 Regional geology 11
1.4 Previous work 17
1.5 Objectives 21
1.6 Methods of Study 22
Chapter 2 Core Descriptions and Facies Analysis 27
2.1 Mannville Group 27
2.1.1 Cantuar Formation 27
2.1.2 Pense Formation 41
2.2 Colorado Group 48
2.2.1 Joli Fou Formation 48
2.2.2 Viking Formation 55
2.2.3 Westgate Formation 58
2.2.4 Fish Scale Formation 61
2.2.5 Belle Fourche Formation 65
IV 2.2.6 Second White Specks Formation 67
2.2.7 Carlile Formation 72
2.2.8 First White Specks Formation 73
2.3 Montana Group 76
2.3.1 Milk River Formation 76
2.3.2 Lea Park Formation 78
2.3.3 Belly River Formation 83
Chapter 3 Stratigraphic Correlation 89
3.1 Introduction 89
3.2 Structure and Isopach maps 91
3.3 Stratigraphic Correlation 100
3.3.1 Mannville Group 100
3.3.2 Colorado Group 102
3.3.3 Montana Group 108
3.4 Depositional Environments and Changes
in Relative Sea-Level 111
Chapter 4 Diagenetic Studies 115
4.1 Introduction 115
4.2 Petrography of sandstones 115
4.2.1 Composition and texture 115
4.2.2 Diagenesis and paragenetic sequence 124
4.3 Organic matter study of shales 139
4.3.1 Rock-Eval analysis results 139
V 4.3.2 Source rock potential 142
4.3.3 Thermal maturity 148
4.4 Stable isotopes of carbonate components 155
4.4.1 Data description 155
4.4.2 Interpretation of the results 159
Chapter 5 Discussion 162
5.1 Sediment sources 162
5.2 Porosity 163
5.3 Implications for hydrocarbon exploration 164
5.4 Recommendation for future studies 166
Chapter 6 Conclusions 168
References 170
Appendix IPL well data retrieved from well tickets 182
VI List of Tables
Table 1 Depth, porosity, and components of the sandstone samples
from the well 3-28-33-23W2 and well 6-18-36-6W3 116
Table2 Rock-Eval analysis results of samples from
Well 3-28-33-23W2 117
Table3 Rock-Eval analysis results of samples
from Well 6-18-36-6W3 118
Table 4 Summary of Rock-Eval data from core samples of
well 6-18-36-6W3 and 3-28-33-23W2 143
Table 5 Hydrocarbon source rock evaluation parameters for
Rock-Eval pyrolysis data 144
Table 6 Results of Carbon and Oxygen Isotope analysis 156
VII List of Figures
1.1 A Map of the distribution of oil and gas fields in Saskatchewan
showing the location of the study area 2
1.2 Location map showing the studied area 4
1.3 The facies belts of the interior Cretaceous sea 5
1.4 Stratigraphic correlation chart of Saskatchewan 7
1.5 Late Cretaceous Sea of North America 12
1.6 Tectonic elements of the Williston and Sweetgrass
Arch region 16
1.7 Location of the two continuous corea studied 24
2.1 Lithofacies of the Mannville Group in well 6-18-36-6W3 28
2.2 Core photos showing various sedimentary structures
of the lower lithofacies association of the Cantuar
Formation in well 6-18-36-6W3 30
2.3 Core photos of the middle lithofacies association of
the Cantuar Formation in well 6-18-36-6W3 31
2.4 Core photos showing various sedimentary structures
of the upper lithofacies association of the Cantuar
Formation in well 6-18-36-6W3 33
2.5 Lithofacies of the Mannville Group in well 3-28-33-23W2 35
2.6 Core photos of the middle lithofacies association of
the Cantuar Formation in well 3-28-33-23W2 36
VIII 2.7 Core photos of the middle lithofacies association of
the Cantuar Formation in well 3-28-33-23W2. 37
2.8 Core photos showing various sedimentary structures
of the upper lithofacies association of Cantuar
Formation in well 3-28-33-23W2 38
2.9 Facies correlation of the Mannville Group
between the two studied wells 40
2.10 Cores photo of Pense Formation in well 6-18-36-6W3 42
2.11 Cores photo of Pense Formation in well 6-18-36-6W3. 44
2.12 Cores photo of Pense Formation in well 3-28-33-23W2 45
2.13 Core photo of Pense Formation in well 3-28-33-23W2. 46
2.14 Core photo of Pense Formation in well 3-28-33-23W2. 47
2.15 Core photo of Joli Fou Formation in well 6-18-36-6W3 49
2.16 Core photo of Joli Fou Formation in well 3-28-33-23W2 51
2.17 Core photo of Joli Fou Formation in well 3-28-33-23W2 52
2.18 Depositional system of Joli Fou and Viking Formation in
studied area 54
2.19 Core photo of Viking Formation in well 6-18-36-6W3 57 56
2.20 Core photos of Viking Formation in well 3-28-33-23W2 57
2.21 Core photos of Viking Formation in well 3-28-33-23W2 60
2.22 Depositional system of Westgate to First White Specks
in studied area 62
2.23 Core photos of Fish Scale Formation in well 3-28-33-23W2 63
IX 2.24 Core photo of Belle Fourche Formation in well 3-28-33-23W2. 66
2.25 Core photo of Second White Specks Formation in
well 6-18-36-6W3 68
2.26 Core photo of Second White Specks Formation in
well 3-28-33-23W2 70
2.27 Core photos of First White Specks Formation in
well 6-18-36-6W3 74
2.28 Core photos of First White Specks Formation in
well 3-28-33-23W2 75
2.29 Core photos Milk River Formation in well 3-28-33-23W2 77
2.30 Core photos of Lea Park Formation in well 6-18-36-6W3 80
2.31 Core photos of Belly River Formation in well 6-18-36-6W3 84
2.32 Core photos of Belly River Formation in well 6-18-36-6W3 86
2.33 Lithofacies associations of the Belly River Formation
ofwell6-18-36-6W6 87
3.1 Map of studied area showing the cross sections 90
3.2 Regional Cross section from southwest Saskatchewan
through central to southeastern Saskatchewan 92
3.3 West-east cross section (B-B')through the study area 93
3.4 Cross section C-C 94
3.5 Cross section D-D' 95
3.6 Cross-section E-E'of the Mannville Group 96
3.7 Mannville structure map of studied area 97
X 3.8 Colorado structure map of studied area 98
3.9 Colorado isopach map of studied area 99
4.1 Classification for sandstones 118
4.2A Quartz-feldspar-lithic grain (QFL) diagram showing
the composition of the framework grains of the
arenite sandstones 119
4.2B Quartz-feldspar-lithic grain (QFL) diagram showing
the composition of the framework grains of the
wacke sandstones 120
4.3 Relationship between depth and porosity of sandstones
from the study area 122
4.4 Photomicrographs showing petrographic
features of sandstones of Cantuar Formation
from well 6-18-36W3 124
4.5 Photomicrograph of sandstone from the Cantuar Formation
of the Well 3-28-33-23W2 125
4.6 Photomicrographs of sandstone of the Cantuar Formation
from the well 6-18-36W3 127
4.7 Photomicrographs of sandstones of the Cantuar Formaation
from well 3-28-33-23W2 128
4.8 Photomicrograph of nonferron radial-fibrous calcite
from well 6-18-36-6W3 129
4.9 Photomicrographs of sandstone of the Cantuar
XI and Belly River 130
4.10 Photomicrographs of sandstones of the Pence Formation
from Well 3-28-33-23W2 and Well 6-18-36-6W3 132
4.11 photomicrograph of sandstone of the Cantuar Formation
of well 3-28-33-23W2 and the Viking Formation
from well 6-18-36-6W3 133
4.12 Photomicrographs of sandstone of the Cantuar Formation
from well 6-18-36-6W3 134
4.13 Photomicrographs of sandstone of Cantuar Formation
from well 3-28-33-23W23-28 135
4.14 Photographs of sandstone of the middle lithofacies
association of the Cantuar Formation in well 6-18-36-6W3 136
4.15 Paragenetic sequence of the Cretaceous sandstone
reservoir in central Saskatchewan 137
4.16 Plot of TOC versus Depth for wells 6-18-36-6W3
and 3-28-33-23W2 141
4.17 Van Krevelen diagram showing kerogen paths and
products of maturation 146
4.18 Plot of H/C vs. O/C of well 3-28-33-23W2
and well 6-18-36-6W3 147
4.19 Plot of Tmax versus Depth for wells 6-18-36-6W3
and 3-28-33-23W2 149
XII 4.20 Schematic relationship of organic matter diagenesis stages 150
4.21 Ro versus Depth of the well 6-18-36-6W3 152
4.22 Plot of Rock-Eval Tmax, TOC and HI versus Depth
of the well 6-18-36-6W3 153
4.23 Plot of Rock-Eval Tmax, TOC, HI versus Depth
of the well 3-28-33-23W2 154
4.24 Carbon vs. oxygen isotopic composition of calcite cement
in central Saskatchewan 157
4.25 Distributions of 513C (%<> VPDB) and 5180 (%o VPDB) with
respect to depth of calcite cements in central Saskatchewan 158
XIII Chapter 1. Introduction
Saskatchewan is the second largest oil producer and third largest natural gas producer among Canadian provinces (Saskatchewan Geological Survey,
2003). The oil is trapped in carbonate and clastic reservoirs ranging in age from
Ordovician to Cretaceous. The natural gas is mainly produced from shallow
Cretaceous clastic reservoirs (Saskatchewan Geological Survey, 2003). Most of the hydrocarbons found within Cretaceous rocks are located in western, southwestern and southeastern Saskatchewan (Fig 1.1), for which there are many geological studies in the literature. Few studies have been carried out on
Cretaceous strata in central Saskatchewan, which seems to be barren of hydrocarbons.
This study aims to characterize the Cretaceous rocks in central
Saskatchewan in terms of stratigraphy, reservoir quality, and source rock potential. The study investigates vertical and lateral changes in sedimentary facies, lithology, diagenetic features and source rock quality in central
Saskatchewan through core logging and sample analysis from two continuous cores penetrating the Mesozoic successions, and places central Saskatchewan into regional context by stratigraphic correlation. The implications of this study for hydrocarbon potential in central Saskatchewan are discussed.
1.1 Study area
Central Saskatchewan has been the most important potash producing
1 MANITOBA
PRINCE "•7. ALBERT Shallow Biogenic Aar\M! OON Gas Williston Basin Light Crude I
Swift Current Medium I MONTANA HGR7HDAKOT
Fig 1.1 A map of the distribution of oil and gas fields in Saskatchewan (from
Yurkowski, 2008) showing the location of the study area.
2 area in Canada since 1942, when intensified petroleum exploration during World
War II led to the discovery of potash deposits near the top of the Middle
Devonian Prairie Evaporite Formation (Saskatchewan Geological Survey, 2003).
The studied area lies along the northwest edge of the Williston Basin (Fig 1.2).
The Williston Basin forms the southeastern extremity of the Western Canada
Sedimentary Basin and has been a major exploration region due to its significant reserves of hydrocarbons (Kent and Christopher, 1994). The Williston Basin is bound by the Sweetgrass Arch to the west, the Sioux Arch to the south, the
Precambrian exposure to the east and the Punnichy Arch to the north (Wallace-
Dudley era/., 1998;, Kent and Christopher, 1994). The study area is located near the east-west trending Punnichy Arch area (Fig 1.2).
McNeil and Caldwell (1981) recognized three north trending facies belts within the Upper Cretaceous of western Canada (Fig 1.3). They are 1) the western facies that consists of coarse grained and sandy lithology, 2) the median facies that consists of shale, silty shale and calcareous shale with minor chalk, limestone and sandstone, and 3) the eastern facies that consists of shale, chalk and limestone. The upper Cretaceous strata within the study area fall within the median facies belt.
1.2 General stratigraphy
The stratigraphic nomenclature used in this study has been defined and studied in the contiguous region of southwest Saskatchewan, west-central
Saskatchewan, southeast Saskatchewan and east-central Saskatchewan. The
3 96°. 102 ,.-?-—\ ALBERTA f^\ SASKATCHEWAN , \ \ ^ \ W^NffOBA i Canadian t ) 1 ^ \ Winnipeg ^49" 9# 12 n Fig 1.2 Location map showing the studied area (Modified from Mossop and Shetsen, 1994) 4 QUI F OF MEXICO MBXICO Fig 1.3 Facies belts of the interior Cretaceous sea (modified after McNeil and Caldweli, 1981) 5 Cretaceous was deposited over a period of 79 m.y., from Berriasian through Maastrichtian, based on the Saskatchewan Stratigraphic Correlation Chart (Fig 1.4) published by Saskatchewan Industry and Resources (2004). The geographic areas in the Stratigraphic Correlation Chart are defined by boundaries along Latitude 52° N and Longitude 106°W. Central Saskatchewan lies in between southwest and southeast Saskatchewan. It covers the northeast corner of southwest Saskatchewan and northwest corner of southeast Saskatchewan. A new stratigraphic chart (Fig 1.4) was created for this study which adopted the nomenclature of southwest and southeast Saskatchewan and incorporated lithostratigraphic and foraminiferal fauna studies (Price and Ball, 1971, 1973; North and Caldwell, 1975; Simpson, 1982) The Lower Cretaceous Mannville Group consists of sandy non-marine to marginal marine deposits (Christopher, 1984a and b) which is the main focus of the reservoir study in this paper. It was deposited in a low-accommodation setting over a long period of time (Leckie etal., 2004) The Mannville Group of central Saskatchewan can be correlated with the Mannville Group in southwest and southeast Saskatchewan. As summarized by Christopher (2003), the name 'Blairmore' was earlier applied to the lower Cretaceous strata, but was replaced by 'Mannville' (Maycock, 1967). It is equivalent to the Swan River Formation of Manitoba. The subdivision of Cantuar and Pense Formations was first proposed by Price (1963). The Colorado Group consists of thick, extensive, predominately marine shale. The Colorado Group was deposited during a major epicontinental shallow 6 Ministry eS fofipdot«s,»e Stratigraphic Correlation Chart •ftiMWiOflfat Rn»«e«t This sludy Tim prowwe s suMwted n*> but g»g^a« as« WW Hr N MttS!tr*em ! Fig 1.4 Stratigraphic correlation chart of Saskatchewan (Saskatchewan Industry and Resources, 2004). 7 marine transgression which occurred worldwide (Williams and Stelck, 1975; Simpson, 1975; Kauffman, 1977; 1984) over a period of 25-30 m.y. (Schroder- Adams, etal., 1996) and is the main focus of the geochemical study in this thesis. Several sandy influxes formed by smaller-order transgressive-regressive cycles within this main transgression are included in the reservoir evaluations. In Saskatchewan, Simpson (1982) subdivided the Colorado Group into Lower Colorado and Upper Colorado at the base of the Second White Speckled Shale. The Lower Colorado Group is composed of, in ascending order, the Joli Fou, Viking, Westgate, Fish Scale and Belle Fourche Formations. The Joli Fou Formation designation was first applied by Wichkenden in 1949 to describe the marine shales on the Athabasca River area between the underlying sandy Grand Rapid Formation (Mannville Group) and the overlying sandy Pelican Formation (Viking Formation) (Price and Ball, 1971). Within the lower beds of the Joli Fou Formation, the Spinney Hill Member is composed of interbedded marine glauconitic shales and fine grained sandstones. The Spinny Hill sandstone attains its maximum thickness of about 34m in west central Saskatchewan and extends southward to the Swift Current area (Simpson, 1975). In the Manitoba Escarpment, the Joli Fou Formation is equivalent to the Skull Creek Member. The Viking Formation was first proposed by Slipper in 1917 (Price and Ball, 1971). The Viking consists of a wedge of sandstone which thins eastward from British Columbia to Saskatchewan. In central and eastern Saskatchewan, the Viking Formation decreases to less than 10m. It is equivalent to the Newcastle Sand in Manitoba (Leckie et. al., 1994). The Westgate Formation was defined by 8 Bloch et al (1993) and is equivalent to the Westgate member of the Ashville Formation in the Manitoba Escarpment (Pedersen, 2004). The Fish Scale Formation is a basin-wide marker that demarcates the Albian/Cenomanian boundary (Lower/Upper Cretaceous). The Belle Fourche Formation was introduced and correlated from the United States Western Interior Seaway to Saskatchewan by North and Caldwell (1975). It is comprised of dark marine shales with a widely recognized "X" bentonite bed (McNeil and Caldwell, 1981) and was reliably dated as Middle to Upper Cenomanian by foraminiferal fauna and bentonite studies (Schroder-Adams etal., 2001). In recent years, some other workers (Bloch etal., 1993; Ridgley etal., 2001) redefined the Belle Fourche and overlying Second White Specks Formations by assigning some calcareous shales to Upper Belle Fourche above the X bentonite. In this study, the former definition of the Belle Fourche Formation as a non calcareous shale with the X bentonite on top is adopted. The Upper Colorado Group consists of Second White Specks, Carlile and Niobrara formations. The Second White Speckled Shale is a basin-wide distinct unit characterized by calcareous shale with abundant white specks that are in white, fine- to very fine-grained sand-sized fecal pellets (Schroder-Adams, etal., 1996). It was deposited during the Late Cenomanian to Middle Turonian over 2.1 my (Schroder-Adams etal., 1996). The Carlile Formation was previously defined to represent middle to Upper Turonian marine non-calcareous shale between the Greenhorn and Niobrara Formations in United States (McGookey etal., 1972). The formation designation was first introduced into the Alberta Southern Plain 9 region and southwest Saskatchewan by Nielsen (2003). The Morden shale in southern Manitoba is equivalent to the Carlile Formation in southwest Saskatchewan (Pedersen, 2003). The Niobrara Formation was formally defined by Nielsen et al (2003) in southern Alberta and southwestern Saskatchewan to describe the Upper Colorado shale. It is comprised of the Govenlock (Verger), Medicine Hat and First White Specks members in southeast and southwest Saskatchewan (Christopher and Yorkoswki, 2004; Pedersen, 2004). Eastwards, the Medicine Hat sand pinches out and only Govenlock and First White Specks Members can be recognized (Fig 1.4). The Montana Group was first defined by North and Caldwell (1975) to represent the shale sequence deposited during Campanian and Maestrichtian in Saskatchewan. It consists of the Milk River, Lea Park, Belly River and Bearpaw Formations. In the study area, the Bearpaw Formation is not present in the two logged cores. The Early Campanian Milk River Formation is a sandy clastic wedge deposited in southern Alberta and Saskatchewan and the southern and central Rocky Mountain Foothills (Mossop and Shetsen, 1994). It contains a large amount of biogenic gas in southwestern Saskatchewan and southeastern Alberta (Pedersen, 2004). A major Late Cretaceous (Campanian) unconformity occurs between the Santonian-Campanian Alderson (Milk River) and the Campanian Lea Park Formation from southwestern to southeastern Saskatchewan (Christopher, 2003). The pre-Lea Park unconformity truncates the underlying strata, deepening to the east, with an erosional relief of about 260m in southern Saskatchewan (Christopher, 2003). The shallow marine shale with 10 minor sandstone interbeds in the Lea Park Formation filled the underlying relief of the Niobrara Formation and even exceeds the accommodation space created by pre-Lea Park erosion in some places (Christopher and Yurkowski, 2003). The Lea Park shale is equivalent to the Pembina member of Pierre Shale Formation in Manitoba Escarpment (Schroder-Adams etal., 2001). The Belly River Formation represents the youngest sand package of the Upper Cretaceous present in the study area and is also included in the reservoir study in this thesis. It is equivalent to the Judith River Formation in northwest Manitoba (Eberth etal., 1990). 1.3 Regional geology "The Western Interior Basin (Fig 1.5) of North America is one of the greatest natural laboratories in the world for understanding the dynamic interactions among tectonic, oceanographic, climate, sedimentologic and biologic factors in the evolution of an ancient, large epicontinental sea" (Kauffman and Caldwell, 1993). The evolution of Cretaceous Western Interior Sea is recorded in the distinct, complex stratigraphic architecture that recorded the sea-level changes (Williams and Steick, 1975; Kauffman and Caldwell, 1993; Beaumont etal., 1993; Stott, 1993). A global sea-level cycle chart showing several first- second order sea level changes was summarized by Kauffman and Caldwell (1993). Each first order sea level cycles includes many higher order sea-level fluctuations (Kauffman and Caldwell, 1993). The transgressive-regressive (T-R) cycles were mainly controlled by eustatic changes in sea level, with water coming from the 11 southern Tethyan Sea and the northern Boreal Sea (Fig 1.5). The Canadian part of the Western Interior Seaway was influenced mainly by southward expanding cold water from the circumpolar regions, whereas the central and south parts in the United States were affected by the northward expanding warm water from the Gulf Coast and Caribbean region (Kauffman and Caldwell, 1993). The records of these changes are preserved in the strata deposited in deep sea, marginal and continental environments. Based on Kauffman and Caldwell (1993) and Willams and Steick (1975), the five second order T-R cycles in the Cretaceous relating to the study area are described below First T-R cycle Early Cretaceous inundation occurred only in the north. From Late Berriasian to Late Early Albian (Upper Cantaur to Pense depositional period), the Arctic Ocean water transgressed the old interior drainage basin and proceeded progressively southward to the latitude of present-day Calgary. Second T-R cycle In the Early Late Albian (Joli Fou to Viking depositional period), the cool northern sea transgressed south into central Colorado, and the warm southern sea overstepped the tectonic barriers of Texas and expanded northward. This brief confluence ended in the Late Albian (Viking deposition time). 12 Fig 1.5 Late Cretaceous Sea of North America (about 75 million years ago), showing the Cretaceous Western Interior Seaway dividing the continent into a western landmass (Laramidia) and an eastern landmass (Appalachia). (Modified from Ron Blakey. 2010) 13 Third T-R cycle (Greenhorn cycle) During Latest Albian- Early Late Turonian (Westgate to Carlile depositional period), the southward transgression of the northern sea formed the Mowry Sea (largest northern sea) which linked to the northward migration of the southern sea. The Greenhorn Cycle is the largest and most globally synchronous cycle. Fourth T-R cycle (Niobrara cycle) The second largest transgression occurred from Early Late Turonion to Middle Early Campanian (First White Specks to Milk River depositional period). It maintained a prolonged interval of peak flooding. The Niobrara T-R Cycle also represents a long period of oxygen depletion and organic carbon accumulation in the Western Interior Basin. Fifth T-R cycle (Claggett cycle) During Campanian time (Lea Park to Belly River depositional period), two similar T-R cycles occurred. These cycles were characterized by widespread deposition of marine sandstone during regression and organic-rich black shale during the maximum flooding interval. The Western Interior Basin experienced asymmetrical and differential subsidence during the Cretaceous (Kauffman, 1977). Four longitudinal tectonic zones were identified and described by Kauffman (1993) in the reconstructed Western Interior Basin. These tectonic zones are, from west to east: 1) the western foredeep which had the highest rate of sedimentation, with 14 deposition dominated by coarse-grained, synorogenic, terrigenous sediments deposited in coastal-plain to shallow marine environments; 2) the broad west-median trough developed along the axis of the foreland basin which was the deepest environment within the basin. The west- median trough had episodic, strong, rapid subsidence resulting in thick accumulations of medium to fine grained sediments. 3) the broad east-median hinge with a moderate to low sedimentation rate and varied subsidence. 4) the east platform was technically stable. The asymmetrical subsidence resulted in the deposition of Cretaceous strata, especially the Colorado group, as an overall eastward thinning wedge shape (Nielsen, 2008). Central Saskatchewan is situated within the east-median hinge zone The tectonic zones play an important role in defining the sedimentation of the studied area, however, the local tectonic adjustment significantly influenced and complicated the stratigraphic architectures (Kauffman and Caldwell, 1993; Leckie et. al., 1994, 1994). The major structural elements affecting Colorado Group deposition in the Western Canada Sedimentary Basin are the Bow Island Arch in Alberta, and the Bowdoin Dome and Swift Current Platform in southern Saskatchewan. Negative structural elements include the Williston Basin, and the Moose Jaw Syncline in southern Saskatchewan (Leckie et. al., 1994). The local tectonic adjustments include the activities of the Punnichy Arch, in which the study area is located, and salt solution structures associated with the Middle 15 126" Tectonic Elements 6s"r NORTHWEST TEBBlTORlES - e~— . . __ ^ r \ ALBERTA SASKATCHEWAN \ A^OB" A Canadian I M \ Shield 1 /O $,' |49* Williston, 96° •^—BSsTn" Kevin-Sunburst * O • P5s * Bowdoin Dome O CO Dome Fig 1.6 Tectonic elements of the Williston and Sweetgrass Arch region (Modified from Leckie etal., 1994 ) 16 Devonian Prairie Evaporite (Simpson, 1982). Tectonic movement on the Punnichy Arch can be traced back to Silurian time, with dramatic post- Mississippian erosion that produced relief of up to 300m (Mossop and Shetsen, 1994). It was re-activated in Early Cretaceous time and also during the Late Albian (Mossop and Shetsen, 1994), and influenced the deposition of Cretaceous strata in central Saskatchewan. The Salt solutions created small-scale basement linear structures that trend northeasterly and northwesterly (Simpson, 1982). 1.4 Previous work Detailed studies of the Cretaceous strata have been carried out in southwestern and eastern to southeastern Saskatchewan (Price, 1963; Christopher, 1974, 1984a and b, 1999, 2000, 2003, 2004; Yurkowski etal., 2006; Pedersen, 2004; Ridgley etal.,, 2001; Nielsen etal., 2003, 2008). Studies in Central Saskatchewan include Price and Ball (1971, 1973), Simpson (1975), North and Caldwell (1975), Christopher (1984, 2003, 2006) Kyser etal. (1993), Stasiuk (1993), Schroder-Adams etal. (1996, 2001), and Wang, etal. ( 2005). Price and Ball (1971, 1973) provided detailed stratigraphic descriptions and microfaunal studies of the Cominco and Duval potash mine shafts (18-36- 6W3 and 11-16-35-8W6) in central Saskatchewan. In these studies, "Blairmore Group" was applied to the twofold basal Cretaceous sandy beds (equivalent to the Mannville Group in this study) that contain the fluvial-deltaic Cantaur Formation at the base and the overlying transgressive marginal marine deposits of the Pense Formation. Lower Colorado sediments were ascribed to the 17 Ashville Group and Upper Colorado sediments were designated as belonging to the Vermillion River Formation. In addition to detailed lithological description, an important unconformity between the Lower Colorado and the Upper Colorado Group was recognized by the single White Speckled shale and the missing non- calcareous Morden dark shale usually found between the lower Second White Specks and the upper First White Specks shales. Price and Ball's studies (1971, 1973) included microfauna studies done by Dr. J. A. Jeletzky and Mr.T.P. Chamney (Geological Survey of Canada). The microfauna indicated that the single White Speckled shale belonged to the First White Specks (Price and Ball, 1973, p. 38). However, the foraminiferal fauna study by North and Caldwell (1975) found that the ammonites and bivalves identified by Jeletzky were found 27-32 feet and 67-72 feet above the base of this single White Speckled shale in the Cominco and Duval mine-shaft sections. The lowest 5-20 feet of green shale- clast conglomerate of the White-Speckled Shale described by Price and Ball (1971, 1973) belonged to the basal beds of Second White Speckled shale distinguished by the fauna species Clavihedbergella (North and Caldwell, 1975). The regional geology of the Lower Cretaceous Mannville Group in Saskatchewan has been discussed by many workers (Price, 1963; Maycock, 1967; Christopher, 1975, 1984, 2003, Leckie etal., 1997a and b). The comprehensive study by Christopher (2003) concluded that the pre-Cantuar topography is controlled by major structural blocks. The fluvial-deltaic Cantuar Formation is a regional blanket with the basal units infilling and covering a topography of valleys and terraces. The marine Pense Formation overlies the Cantuar Formation on a 18 relatively flat planar disconformity (Christopher, 2003). The Cretaceous Colorado Group consists predominantly of marine shales interspersed with relatively thin sandstone and conglomeratic beds and minor shaly chalk, chalky limestone, bentonite, pelecypod coquinas, horizons of fish debris, nodular phosphorite, and siderite, calcite and pyrite concretions (Mossop and Shetsen, 1994). The Colorado Group was deposited in a dynamic and variable basin setting during an overall eustatic sea-level rise punctuated by sea level falls due to local tectonic activities (Schroder-Adams etal., 1996). The Colorado Group is of significant economic importance in that it contains about 14 percent of the total Western Canada hydrocarbon reserves (Podruski et al., 1988; Porter, 1992). Simpson (1975), North and Caldwell (1975), Kyser, etal. (1993) and Schroder-Adams etal. (1996, 2001) studied the paleoenvironmental changes, geochemical features and foraminifera assemblages of the Cretaceous strata in Saskatchewan. According to the above mentioned regional studies, the paleoenvironments of the Upper Cretaceous are distinctly different between western, central and eastern Saskatchewan, resulting in differences in lithology, total organic carbon content (TOC), oxygen and carbon isotopes, and faunal assemblages. North and Caldwell (1975) distinguished sixteen foraminiferal assemblage zones from the western Saskatchewan Cretaceous sequence and nine from the eastern Saskatchewan Cretaceous sequence. In the study of North and Caldwell (1975), a reliable biostratigraphic correlation of the two sequences and extensive biostratigraphic correlations to Cretaceous rocks in the U.S. were carried out. 19 Each zone of Cretaceous strata was placed into an age equivalent context and three important unconformities occurring during the Late Albian- Early Campanian were recognized guided by faunal assemblage recognition. Unconformities exist between the Fish Scale and Belle Fourche Formations, between the Belle Fourche and Second White Specks Formations, and between the Second White Specks and First White Specks Formations, resulting in a thin pre-Campanian sequence (North and Caldwell, 1975). Another unconformity, pre-Lea Park unconformity, was formed during the early Campanian (Christopher and Yurkowski, 2003). From southwest to southeast Saskatchewan, the pre-Lea Park strata (Milk River Formation) thinning to the east is partly in response to internal disconformities and partly due to the pre-Lea Park unconformity increasingly truncating the underlying sediments to the east (Christopher and Yurkowski, 2003). As previously discussed, central to eastern Saskatchewan lies within the east-median hinge tectonic zone, where the Upper Cretaceous strata are dominated by marine shale with fossils. Two transgressive-regressive marine cyclothems in this area, the middle Cenomanian-middle Turonian Greenhorn cycle and the early to middle Campanian Claggett cycle, have been identified as favourable for the study of paleoenvironmental geochemistry (Kyser, et al., 1993). The carbon and oxygen isotope study of aragonite, calcite and phosphate from fossil material recovered from the Potash mine shaft-Gerald section in southeast Saskatchewan indicates that the 5180 value of the Greenhorn Sea was very low during late Cenomanian and early Turonian time, but both 6180 and 513C 20 increased dramatically as Cenomanian gave way to Turonian time (Kyser etal., 1993). The low 6180 is interpreted to indicate that the Greenhorn Sea contained substantial components of meteoric water (Kyser etal., 1993). The carbon and oxygen isotope study of calcite and phosphate from fossil materials of Lea Park Formation recovered from the Potash mine shafts-Dual and Vascoy sections in south-central Saskatchewan indicates that the 6180 values are lower than the 18 normal Claggett seawater 5 0 value of -1.0% 0 (Shackelton and Kennett, 1975) and suggests that it was modified by water with a lower 5180 value than seawater (Kyser etal., 1993). 1.5 Objectives The review of previous work indicates that the Cretaceous rocks in central Saskatchewan have been studied to variable degrees for different formations and different topics. However, it has not been well understood, taking into account the whole Cretaceous, how the stratigraphy and facies are distributed, how central Saskatchewan is correlated to western and eastern Saskatchewan, what the reservoir quality and the source rock potential is, and what are the implications of the above are to hydrocarbon exploration. This study is a detailed examination of the stratigraphy, sedimentology, diagenesis and geochemistry of Cretaceous strata in central Saskatchewan The main objectives are: 1) Facies analysis: examine continuous potash mine cores to identify the depositional environments of each formation and their relationship to sea- 21 level changes. Facies will be defined based on lithological associations, sedimentary structures, trace fossils and references from previous regional environmental studies. 2) Stratigraphic correlation: integrate core logging and wireline log correlation to create one regional cross section from western to southeastern Saskatchewan to determine how the strata varies laterally and the controlling factors. In addition, several local cross sections will be created to help understand the stratal distribution. 3) Petrographic and diagenetic study of sandstones: classify the sandstones by point counting and study diagenetic features by observing thin sections under the microscope in order to understand the post depositional diagenetic processes and their influence on reservoir characteristics and quality. 4) Geochemical study of shale: analyze shale samples with the Rock-Eval pyrolysis method to evaluate the hydrocarbon-generative potential of Cretaceous marine shale in the study area. The quantity, kerogen types, thermal maturation and diagenetic stage of the organic matter will be studied. 5) Stable isotopes of carbonate cements: analyze carbon and oxygen isotopes from carbonate cements to help understand the diagenetic conditions. 1.6 Methods of study Methods used in this study include core logging for lithological descriptions and facies analysis, point counting and petrographic examinations of thin sections with a petrographic microscope, construction of cross sections, 22 Rock-Eval analysis of organic matter in shales and analysis of isotope data from carbonate components. Two continuous cores, located in 3-28-33-23W2 and 6-18-36-6W3 from the potash mine area near Saskatoon were examined (Fig 1.7). Eight hundred and two wireline log raster images in the study area from the MJ LogSleuth database were examined. About 460 wells were used to make structure maps and isopach maps of the Mannville and Colorado Groups. The industry tops and thickness of the Mannville and Colorado groups were retrieved from well tickets in GeoScout (Appendix 1). The two wells examined, 3-28-33-23W2 and 6-18-36- 6W3, have continuous core coverage of Cretaceous strata from, in ascending order, the Lower Cretaceous Mannville Group, the Lower to Upper Cretaceous Colorado Group, and the Upper Cretaceous Montana Group. The Mannville Group represents the thickest sandstone interval within the Cretaceous succession, although the Viking and Belly River Formations also contain sandstone deposits. These strata are the focus of the reservoir studies, which will examine porosity changes with depth, petrographic features, diagenetic processes and their influences on reservoir qualities. Two hundred and four samples were taken from the two wells for petrographic and geochemical studies. Ninety of them were taken to make petrographic thin-sections. The thin sections were made by Vancouver Petrographies Ltd. in Langley, B.C. Some of the samples were used for both making thin sections and analyzing isotope content. Fifty-five samples were taken for Rock-Eval 6 pyrolysis. Among many 23 Saskatoon • Gas .* • Oil 6-18-36^6W3 -* • 3-28*33-23W?, • *!•• Jr<9, * '. '. s CD Study area - „ c CO W Regina Moose Jaw « if ! Fig 1.7 Location of the two continuous cores studied. 24 pyrolysis methods, Rock-Eval pyrolysis has been widely used in the industry as a standard method in petroleum exploration (Lafargue, et al., 1998). Firstly, the samples were ground into powder, with every sample containing at least 100 mg of powder. Then the samples were isothermally heated in an inert atmosphere (Helium or Nitrogen) to quantitatively and selectively determine the following parameters (Pimmel and Claypool, 2001) S1: the amount of free hydrocarbons (gas and oil) in the sample, reported as milligrams of hydrocarbons per gram of the rock (mg HC/g Rock). S2: the amount of hydrocarbons generated through thermal cracking of non volatile organic matter. S2 is an indication of the quantity of hydrocarbons that the rock has the potential to produce. S3: the amount of CO2 produced during pyrolysis of kerogen. S3 is an indication of the amount of oxygen in the kerogen and is used to calculate the oxygen index. Tmax: the temperature at which the maximum release of hydrocarbons from cracking of kerogen occurs during pyrolysis (top of the S2 peak). Tmax is an indication of the stage of maturation of the organic matter. TOC: the total organic carbon; it is determined by oxidizing the residual organic carbon after pyrolysis to detect the organic matter remaining in the sample. Hydrogen index (HI = [100 x S2]/TOC): the quantity of hydrocarbon from S2 relative to the total organic carbon. Oxygen index (Ol = [100 x S3]/TOC): the quantity of carbon dioxide from 25 S3 relative to the total organic carbon. Production index (PI = S1/ [S1 + S2]): to indicate the evolution level of organic matter. Calcite cementation is an important diagenetic component of siliciclastic rocks in central Saskatchewan. Fifteen samples of carbonate cements were analyzed for carbon and oxygen isotopes. The bulk samples were used, as it is difficult to separate the carbonate cements from sandstones. The samples were crushed with a mortar and pestle. The samples were sent to the University of Saskatchewan in Saskatoon for carbon and oxygen isotope analysis. In the lab, carbonate-cemented samples are roasted in a vacuum oven at 200°C for 1 hour to remove water and volatile organic contaminants that may obscure the stable isotope values of the samples. Stable isotope values were obtained using a Finnigan Kiel-Ill carbonate preparation device directly coupled to the dual inlet of a Finnigan MAT 253 isotope ratio mass spectrometer. 20-50 micrograms of carbonate were reacted at 70°C with 4 drops of anhydrous phosphoric acid for 240 seconds. Isotope ratios were corrected for acid fractionation and 170 contribution and reported in per mil notation relative to the V-PDB standard. Precision and calibration of data are monitored through routine analysis of the 13 18 IAEA NBS-19 standard. Standard deviations for 5 C and 6 0 are 0.05%o and 0.10%o, respectively (one sigma). 26 Chapter 2. Core Descriptions and Facies Analysis The two wells examined, 3-28-33-23W2 and 6-18-36-6W3, both have continuous core encompassing, in ascending order, the Lower Cretaceous Mannville Group, the Lower to Upper Cretaceous Colorado Group, and the Upper Cretaceous Montana Group. With the exception of the Mannville Group, the Viking Formation of the Colorado Group, and some sandy intervals in the Belly River Formation of the Montana Group, the majority of the Cretaceous strata in central Saskatchewan are composed of shales. The Mannville Group represents the thickest sandstone interval within the Cretaceous succession. 2.1 Mannville Group The lithofacies characteristics of the Mannville Group, described below, are based on core logging of the 6-18-36-6W3 and 3-28-33-23W2 wells. The Cantuar and Pense formations are described separately. 2.1.1 Cantuar Formation 2.1.1.1 Well 6-18-36-6W3 In well 6-18-36-6W3, the Cantuar Formation is divided into three lithofacies associations (Fig. 2.1). 27 Cretaceous Colorado Mannville Group Group , Cantuar Fro s Lower htdofscies association Middle lithofacies association Upper lithofacies association Pense Era Jj*Fo«Fm| « ti % ^ < r li a < 5- o ^a^oS^SBlg. S. Q. to Q. 3 A) Lower lithofacies association: 577.0-569.4m: Very fine-grained sandstone, argillaceous, friable, cross-bedded (Fig. 2.2A) with a 0.46m coal seam in the upper part. Sharp basal contact with carbonates of the underlying Birdbear Formation. 569.4-565.1 m: Characterized by very fine-grained sandstone with burrows, more argillaceous upwards; planar and trough cross-bedding common in lower part, lenticular bedding and planar lamination dominant in the upper part; synaeresis cracks present in the upper part (Fig. 2.2B). 565.1-552.3m: Five beds of white, very fine-grained sandstones interbedded with thin dark mudstones and coal seams, upward increase in bioturbation (Fig.2.2C) except in the basal sandstone; ripple cross-beddings, ripple cross- lamination and lenticular bedding common (Fig. 2.2D). B) Middle lithofacies association 552.3-545.6m: White, medium-grained massive quartzose sandstone with grains of dark chert, poorly sorted, hard, fining upwards, planar bedding (Fig.2.3A) and ripple lamination in upper portion; basal contact sharp and angular (Fig.2.3B). 545.6-535.8m: Light gray and dark gray shale interbedded with argillaceous siltstone, abundant burrows (Fig. 2.3C) and plant fragments (Fig.2.3D); planar lamination and ripple cross-bedding, and 29 1 2 3 4 5 6 CENTIMETRES Fig 2.2 Core photos showing various sedimentary structures of the lower lithofacies association of the Cantuar Formation in well 6-18-36-6W3. A. Very fine-grained cross-bedded sandstone,; B. Synaeresis cracks (567.0m); C. Intensely bioturbated muddy sandstone (553.5m); D. Ripple cross-lamination (558.6m). 30 Fig 2.3 Core photos of the middle lithofacies association of the Cantuar Formation in well 6-18-36-6W3. A. Low-angle planar lamination (549.2m); B. Sharp basal contact of the middle lithofacies association (552.3m); C. unknown Burrows (544m); D. Plant fragments on bedding plane (536.4m). 31 syndepositional deformation structures 535.8-529.4m: Very fine-grained sandstone, uncemented, massive, grading upward to light gray mudstone interbedded with thin argillaceous siltstone. C) Upper lithofacies association 529.4-523.6m: Calcareous, interbedded siltstone and mudstone fining upward to light gray mudstone; pyrite concretions, syndepositional deformation structures, lenticular bedding and ripple lamination common in the lower sandy portion. 523.6-515.1m: Several thin, argillaceous siltstone beds in the base grading to light gray silty mudstone; almost all of the beds in the interval intensely bioturbated; cross-bedding common in the lower silty part, and planar lamination and ripple cross-stratification dominant in the upper part. 515.1-509.6m: Two fining-upward successions consisting of very fine-grained sandstone grading to siltstone or silty claystone, followed by an upward-coarsening succession (0.5m) from claystone to siltstone and then by an interval of dark gray mudstone; planar lamination, bioturbation, carbonaceous fragments; strongly distorted bedding (Fig.2.4A) in the middle interval. 509.6-498.0m: Calcareous, very fine-grained sandstones, thick-bedded, with oxidized iron strips and ripple cross-bedding. 32 OEfSJTJMETR Fig 2.4 Core photos showing various sedimentary structures of the upper lithofacies association of the Cantuar Formation in well 6-18-36-6W3. (A) Deformation structure (512.7m); (B) Sandstone with abundant sphaerosiderite (493.9m). 33 498.0-493.Om: Fining-upward succession with the basal sandstone containing many sphaerosiderite (Fig.2.4B) overlain by weakly indurate argillaceous, very fine-grained sandstone. 2.1.1.2 Well 3-28-33-23W2 In the 3-28-33-23W2 well, the lower lithofacies association presented in the 6-18-36-6W3 well is missing, and the other two equivalent lithofacies associations exhibit distinct characteristics (Fig.2.5), which are described below. A) Middle lithofacies association 502.3-474.2m: Pale, fine-grained sandstone, massive, friable and well sorted, interbedded with several thin beds of oxidized mudstone (Fig 2.6); sedimentary structures dominated by low-angle to high-angle planar cross bedding; ripple cross - lamination (Fig.2.7) in the upper part of the sandstone interval. The basal sandstones are composed of three upward-fining sandstone successions, each 45cm thick, grading from medium-grained sandstone to very fine grained sandstone; sharp contact with underlying coal seam. B) Upper lithofacies association 474.2-447.Om: Composed of five fining-upwards cycles, each consisting of sandstone in the lower part and mudstone in the upper part. Some bioturbation was seen in the lower portion (Fig.2.8A). Plant 34 (Q no en Cretaceous Mannville Group TJ Q. 03 O CD' Cantuar Fm C/3 o Middle lithofacies association CD K 03 3 <3 CD I °° O co CO o i c hO CO CD 00 rb 00 CO 00 ro oo —1 ro I a < 0 ^ / II 1 JJ o g> OS S b % J jpl e s? £ 5" » tur b £ ¥ w. 3 CD 3. 03 3 Q. = CO cF CD bed c stio n ed d o ar b CO =5 CD CD 3 3- X Q. tD Q- ^ Fig 2 6 Core photos of the middle lithofacies association of the Cantuar Formation in well 3-28-33-23W2 Fine-grained sandstone, massive, friable and well sorted, sandstone interbedded with several thin beds of oxidized mudstone. 36 \% Fig 2.7 Core photos of the middle lithofacies association of the Cantuar Formation in well 3-28-33-23W2, showing ripple cross- lamination (474.3m). 37 Fig 2.8 Core photos showing various sedimentary structures of the Upper Lithofacies of the Cantuar Formation in well 3-28-33-23W2. A. Bioturbation in silty mudstone (470.6m); B. Faulted sphaerosideritic sandstone (458.4m). 38 fragments, iron stains and sphaerosiderites, and small scale faults were observed (Fig.2.8B). Interpretation The Cantaur Formation of the Mannville Group in the study area is interpreted as formed in a fluvial-deltaic depositional system. The lower lithofacies association in the well 6-18-36-6W3 is interpreted as the transition zone from subaerial delta plain to subaqueous delta plain. The distributary channel sandstone without trace fossils and the coal seams indicate subaerial environments, whereas the distributary channel sandstone and the dark shale with abundant burrows represent subaqueous environments. The lower lithofacies association is not present in the eastern well 3-28-33-23W2 (Fig.2.9). The middle lithofacies association in well 3-28-33-23W2 shows typical fluvial channel deposits. The three upward-fining successions are interpreted as point bar deposits separated by interfluve mudstones, where the red color indicates subaerial exposure. The succession shows an upward decrease in the scale of sedimentary structures, from cross bedding to ripple bedding, and a decrease in thickness of individual sandstone beds likely reflecting the infill of a channel. In well 6-18-36-6W3, the middle lithofacies association is interpreted as delta plain deposition. The basal sandstone bed is interpreted as a distributary channel deposit which is overlain by flood plain deposits. The flood plain deposits are characterized by mudstone and silty mudstone, with intercalated current ripples, and thin sandstone beds interpreted as crevasse splay deposits (Fig.2.9). 39 3-28-33-23W2 6-18-36-6W3 Bioturbation Sandstone Ripple bedding Lenticular bedding Siltstone Cross bedding Shale Shale interbed Coal Plant fragment Clayclast Iron stains Pyrlte Sidente Fig 2.9 Facies correlation of the Mannville Group between the two studied wells. The datum used is the first flooding surface within the Joli Fou Formation. Note the more marine influenced deposits in well 6-18-36-6W3. 40 The upper lithofacies association exhibits characteristics of delta plain deposits in both wells; with each fining-upwards succession interpreted as distributary channel deposits overlain by fine-grained inter-distributary deposits (Fig.2.9). The western well shows more indications of a marine influence than the eastern well by the intense bioturbation by marine trace fossils, such as Teichichnus, in well 6-18-36-6W3 compared to well 3-28-33-23W2. The coarsening upwards succession is interpreted as distributary mouth bar deposits, indicating that the western area was located in the updip edge of the delta front. 2.1.2 Pense Formation 2.1.2.1 Well 6-18-36-6W3 493.0-489.5m: shale, medium grey, blocky, with ripple beddings and lenticular beddings, horizontal burrows; sharp contact with underlying Cantaur Formation by a thin layer of hard oxidized very fine to silty sandstone with erosional surface at bottom. 489.5-489.3m: sandstone: grey, very fine grained, cross bedded (Fig 2.10), some clay clasts. 489.3-487.Om: shale: medium grey, blocky, sandy, ripple and lenticular bedding, bioturbated. 487.0-485.5m: sandstone and shale interbedded: sandstone-very fine grained, calcareous; shale-medium grey, non calcareous; the whole interval strongly bioturbated. 41 Fig 2.10 Cores photo of the Pense Formation in well 6-18-36-6W3 showing very fine grained cross bedded sandstone (489.5m) 42 485.5-482.5m: sandstone: medium to coarse grained, coarsening upwards (Fig 2.11), calcareous, lenticular bedding in lower portion, ripple bedding in upper portion, muddy in places. 482.5-481.7m: sandstone and shale interbedded: three thin layers of sandstone, very fine to medium grained, cross bedded, calcareous and pyritic in top sand layer; two thin layers of shale, medium grey, sandy. 481.7-479.5m: shale: medium to dark grey, blocky, non calcareous, no bioturbation. 2.1.2.2 Well 3-28-33-23W2 447.0-446.5m: siltstone, medium to dark grey, blocky, hard, strongly bioturbated, with thin siderite concretion layer forming sharp basal contact (Fig 2.12), abundant trace fossils-P/a/7o//tes (Fig 2.13/ 446.5-446.Om: shale, dark grey, blocky, silty. 446.0-442.1m: interbedded shale and siltstone, shale: dark grey, non calcareous; siltstone: filling burrows, ripple and lenticular bedding, abundant trace fossWs-Teichichnus (Fig 2.14A). 442.1-437.7m: siltstone and shale interbedded, siltstone: light grey, cross bedded; shale: dark grey, abundant burrows filled by siltstone, trace iossWs-Terebellina (Fig. 2.14B); cross bedded siltstone truncated by shale. 43 in^Mcji^ntNkMmmV .#TOJa.-«SK.-« CENTIMETRE'S" yt-M •Hsr*-. Fig 2.11 Core photo of the Pense Formation in well 6-18-36-6W3: medium to coarse-grained sandstone, coarsening upwards. 44 S$& v** f' St J > ;* * • V .* ? •* i . J •• . • '** cV,'i7-,a*' •" • «•" * >*.«• v- .-- • "T^S^""* •••• *. * T> * iSf^H Fig 2.12 Core photo of the Pense Formation in well 3-28-33-23W2 showing sandstone with abundant siderite concretions, which is medium to dark grey, blocky, hard, strongly bioturbated, forms sharp basal contact of Pense Formation with underlying Cantaur Formation (447.8m). 45 Fig 2.13 Core photo of the Pense Formation in well 3-28-33-23W2 showing interbedded very fine sand bed and intensely bioturbated mudstones with abundant trace fossils-P/ano//tes (447.3m). 46 UI Fig 2.14 Core photo of the Pense Formation in well 3-28-33-23W2 showing interbedded siltstone and shale with abundant trace fossils- A. Teichichnus (443.8m). B. Terebellina and Teichichnus (442.1m) 47 Interpretation The Pense Formation was deposited during the first T-R cycle as outlined in the introduction chapter. The sea transgressed into the study area during the Pense depositional time, with delta front and prodelta marine (Fig 2.9) conditions prevailing. In well 6-18-36-6W3, the basal contact with the underlying Cantuar Formation is marked by a sharp ravinement erosional surface. In well 3-28-33- 23W2, the contact is overlain by a lag of siderite concretion clasts winnowed from the underlying Cantuar sphaerosideritic sandstone. Above the basal contact, dark shale interbedded with siltstones with abundant trace fossils present in both wells represents a transgressive condensed deposit. The medium to fine grained coarsening upwards sandstone and the muddy siltstone in the upper portions of the two logged wells indicate regressive deposition. 2.2 Colorado Group 2.2.1 Joli Fou Formation 2.2.1.1 Well 6-18-36-06W3 479.5-479.4m: shale with chert clasts, sharp contact with underlying shale (Fig 2.15A) 479.4-477m: shale: dark grey, fissile, noncalareous, interbedded with slightly silty, glauconitic mudstone and calcite strip-pelecypod. 477.0-476.8m: siltstone: light grey, glauconitic, pelecypod strip (Fig 2.15B) 48 Fig 2.15 Core photo of the Joli Fou Formation in well 6-18-36-6W3. A. Chert clasts, sharp contact with underlying shale (479.5m); B. Glauconitic, pelecypod strip (477m) 49 476.8-459.5m: shale: dark grey, platy to fissile, glauconitic, noncalcareous, laminations of light grey, glauconitic siltstone. 459.5-449.Om: shale: medium grey, noncalcareous, laminations and small lenses of very fine grained sandstone in places. 2.2.1.2 Well 3-28-33-23W2 437.7-431 m: shale, dark grey, blocky, sharp contact with underlying siltstone. 431-429.2m: siltstone, green, blocky, glauconitic, thin pelecypod layer through siltstone. 429.2-426m: shale, dark grey, blocky to flaky, non calcareous, glauconitic, silty. 426-425.2m: sandstone, green, very fine grained, glauconitic, crossbedded (Fig 2.16A). 425.2-422m: shale, dark grey, blocky, non calcareous. 422-416.0m: interbedded shale and siltstone; shale: dark grey, non calcareous; siltstone: light grey, muddier upwards, bioturbated and trace fossils (Fig2.16B) in places. 416-414.8m: shale, dark grey, blocky to flaky, non calcareous, horizontal burrows. 414.8-411.2m: shale and siltstone interbedded; shale: dark grey, blocky, non calcareous; siltstone, light grey, flaky, filling horizontal burrows. 411.2-411.1m: bentonite, cream white, abundant mica, calcareous (Fig 2.17A). 411.1-410.3m: shale: dark grey, blocky, non calcareous. 410.3-407.5m: shale and sandstone interbedded (Fig 2.17B); shale: dark grey, flaky, non calcareous; sandstone: light grey, very fine grained, 50 0 1 2 3 4 5 6 7 CENTIMETRES mm- '• J% " -V'. ' * Fig 2.16 Core photo of the Joli Fou Formation in well 3-28-33-23W2. A. Green very fine grained, glauconitic, crossbedded sandstone (426m). B. Horizontal trace fossils (420.5m) 51 CD +± C o c CD CD CD . C • CO CM T3 ^ C CO CO CO 00 CO 00 CD ^To co -C _ CO CD m c C T- O i- si p§ 3o LL CD 3 CO o co LL o CO" CD o 3 a JL3 lAi IJL iM zJ **J 0 12 3 4 5 6 £ E CENTIMETRES „ (fl c •*— >- CO • O c • r^O Q.-Q i- CD "IS o 2 "^ Q|o i- c CD w i-s D3 CD S LL O .£ sandier upwards, abundant horizontal and sub-vertical burrows. 407.5-406.5m: shale, dark grey, blocky, non calcareous, horizontal burrows and shell debris. 406.5-404.7m: shale and siltstone interbedded; sandier upwards, some burrows, lenticular bedding in upper portion. 404.7-404.6m: sandstone, light grey, very fine grained, sharp contact at bottom. 404.6-403.0m: shale, dark grey, speckled sand; pyrite concretions, shells and burrows seen in places. Interpretation The Joli Fou Formation is interpreted as deposited in an offshore marine environment (Fig 2.18). It represents the first inundation of the interior seaway in Late Early Albian (Williams and Steick, 1975). The initial transgression led to deposition of a thin (3-5m) dark shale sharply contacting with the underlying Pense Formation. The green glauconitic siltstone with pelecypod debris immediately above this thin transgressive shale is equivalent to the Spinny Hill sandstone. Simpson (1975) interpreted the Spinny Hill sand to have been deposited in an estuarine delta that extended from southeast of the Prince Albert National Park to the Swift Current area (Simpson, 1975). In south central Saskatchewan, the very thin (0.2-0.6m) glauconitic siltstone is a distal fluvial- marine deposit, indicated by progressive fining and thinning of the sand body with increasing distance from the axis of the Spinny Hill marine sand body (Simpson, 1975). The silty deposits pass upwards into the Joli Fou offshore 53 03 Tl CD CQ" » ro 00 a CD T3 O I CO O 00 3 03. CO CO O) CO CO CD 00 3" CD c_ O O c 03 3 I Q. {/) O O T) <$Q !?S CD L13 ID 0 00 ro c < n 8 5 (5" 3 03 3 03 ST -cr a> ro 3" CO ddin g rbe d din g 5>S beddi n 2 0 00 CQ 55 0 0 03 3 CO 00 CD CO c a. deposits, which are comprised of dark shale with sporadic siltstone filled burrows. Most of the burrows are horizontal and subvertical, indicating a low energy, deepwater environment. The pyrite concretions, Inoceramus, Zoophycos and Schanbcylindrichnus trace fossils on the top portion of the well 3-28-33-23W2 indicate a low energy environment with low oxygen levels. 2.2.2 Viking Formation 2.2.2.1 Well 6-18-36-6W3 449-448.8m: siltstone: grey, argillaceous (Fig 2.19), faint horizontal burrows. 448.8-440.Om: shale: medium grey, non calcareous. 440.0-439.5m: siltstone: grey, argillaceous. 2.2.2.2 Well 3-28-33-23W2 403- 402.95m: conglomerate: 5cm thick, black, cherty grains, grain size ranging from 1-1.5cm, rounded; black and pyritic shale as matrix (Fig 2.20A). 402.95-401.1m: sandstone: light grey, blocky, medium to very fine grained; cross bedding and current bedding, fining upwards, abundant burrows including horizontal, parallel and vertical burrows (Fig 2.20B). 401.1-400.9m: sandstone: light grey, medium to very fine grained, fining upwards, chert clasts at bottom. 55 ?m \-h:i' rs» '("•&». m . .. -SW Fig 2.19 Core photo of the Viking Formation in well 6-18-36-6W3. Siltstone: grey, argillaceous with faint horizontal burrows (449-448.8m) 56 1-. > -^ - V5*' Fig 2.20 Core photos of the Viking Formation in well 3-28-33-23W2. A. Conglomerate: 5cm thick, black, cherty granules, grain size ranging from 1-1.5cm, rounded; black and pyritic shale as matrix (403m). B. muddy very fine grained sandstone with abundant burrows including horizontal, parallel and vertical burrows (402.6m). 57 Interpretation The Viking sandstone marked the first regressive pulse of the Colorado Group. In the well 03-28-33-23W2, the basal contact is a thin chert layer (5cm), representing transgressive lag deposits. The vertical burrows in cross bedded Viking fining-upwards sandstones indicate a high energy level, frequently current- influenced environment, and is likely deposited in a tidal channel. To the west, in the well 06-18-36-6w3, the Viking formation is progressively finer and muddier, indicating a quieter and lower energy environment of proximal-shelf deposition. Viking sand in south central Saskatchewan is interpreted as tidal channels in a nearshore to proximal-shelf depositional environment (Fig 2.18). 2.2.3 Westgate Formation 2.2.3.1 Well 6-18-36-6W3 439.5-423.Om: shale: medium grey, platy to fissile, non calcareous, sandy in places. 423.0-416.5m: shale, light grey, platy to fissile, non calcareous, slightly bioturbated. 416.5-415.9m: sandstone, light grey, very fine grained sandstone, crossbedding; sharp contact with underlying shale. 415.9-414.8m: shale, light grey, platy to fissile, horizontal burrows. 414.8-414.7m: sandstone, light grey, very fine grained, crossbedded. 414.7-414.0m: shale, light grey, non calcareous. 414.0-413.9m: siltstone, light grey, argillaceous, bioturbated. 58 413.9-410.0m: shale, light grey, non calcareous, platy to fissile. 410.0-409.95m: bentonite, cream to light grey. 409.95-405.8m: shale, medium grey, non calcareous, platy to fissile; silt-filled horizontal burrows, intensive upwards, silty upwards. 405.8-404.2m: shale, medium grey, platy to fissile, non calcareous. 2.2.3.2 Well 3-28-33-23W2 400.9-399.3m: shale, light grey, blocky, silty, abundant burrows. 399.3-392.0m: shale, dark grey, blocky, some fish bones in lower portion, rare pyrite nodules; horizontal burrows filled by sand. 392.0-388.7m: shale and siltstone interbedded, shale: dark grey, blocky to platy, non calcareous, bioturbated by Terebellinas (2.21 A); siltstone: 2cm thick (at 391 m), calcareous. 388.7-383.6m: shale and siltstone interbedded, shale: dark to medium grey, blocky to fissile, non calcareous; siltstone: light grey, scattered speckled silts filling burrows, strong bioturbation, sandier upwards cycles in middle and upper portion, rich in fish scales and bones (Fig 2.21 B). Interpretation The Westgate Formation marks the second major transgressive phase of the Colorado Group following the Viking regressive pulse (Schroder-Adams etal., 1996). The predominant dark to medium shale interbedded with normally graded 59 if*- •CO 00 |U"> '*sf LU Fig 2.21 Core photos of the Westgate Formation in well 3-28-33-23W2. A. Trace fossils: Terebellinas (389m); B. Fish scales and bones (388.4m) 60 thin siltstone beds indicates deposition in a distal offshore environment (Fig 2.22) between fair-weather and storm wave base. In the eastern well 3-28- 33-23W2, the intensive bioturbation and presence of abundant horizontal trace fossils likely indicates a well-oxygenated open marine environment. The minor to absent bioturbation in the western well 06-18-36-6W3 indicates a hostile anoxic bottom water conditions. The several sharp-based, cross bedded, very fine grained thin sandstone beds in the Upper Westgate Formation of both wells likely represents distal or low intensity storm events. 2.2.4 Fish Scale Formation 2.2.4.1 Well 6-18-36-6W3 404.2-398.Om: shale, medium to dark grey, platy to fissile, non calcareous; abundant fragments of fish scales, fish bones and teeth. 398.0-397.Om: shale, medium grey, silty, non calcareous.397.0-388.5m: shale, medium to dark grey, platy to fissile, non calcareous; abundant fragments of fish scales, fish bones and teeth; horizontal burrows. 2.2.4.2 Well 03-28-33-23W2 383.6-383.2m: sandstone, light grey, very fine grained, strongly bioturbated, sharp contact with underlying shale with mud clasts at bottom (Fig 2.23A) 61 6-18-36-6W3 3-28-33-23W2 t .anile Fm" I "5 I | g B | U_ Ll_ 380 " I m o -S o o Viking Fm Legend Bioturbation Fynte Rpple bedding Sid 3d e rite Lenticularbedding Sandstone Cross bedding Shale interbed LJ Sltstone Rantfragment Shale Clayclast Coal 01 Glauconitic Iron stains Shell debris ^ Bentonite Fish scale Fig 2.22 Depositional system from Westgate to First White Specks in the study area 62 Fig 2.23 Core photos of the Fish Scale Formation in well 3-28-33-23W2. A. Light grey, very fine grained sandstone, strongly bioturbated, sharp contact with underlying shale with mud clasts at base (383.6-383.2m); B. Very fine grained, muddy sandstone, brown stains (377.9m). 63 382.2-377.9m: shale, dark grey, block to fissile, pyritic, non calcareous. 377.9-377.8m: sandstone: grey green, very fine grained, muddy, brown stains, petroliferous odour (Fig 2.23B). 375.5-370.1m: shale, medium to dark grey, intensively bioturbated, sand distribution speckled due to bioturbation. 370.1-369.9m: shale and siltstone interbedded; shale: dark grey, non calcareous; siltstone: light grey, calcareous; strongly bioturbated. 369.9-350.2m: shale, medium to dark grey, blocky, non calcareous, bioturbated, some fish scales. Interpretation The Fish Scale Formation was deposited during continued transgression (Schroder-Adams etal., 1996) in an offshore environment (Fig 2.22). In the western well 06-18-36- 6W3, the boundary between the Fish Scale Formation and underlying Westgate Formation is a thin layer containing abundant debris of fish scales, bones and teeth. In the eastern well 03-28-33-23W2, the strata graded from Westgate to Fish Scale Formation. The abundant "escape" vertical burrows in the well 03-28-33-23W2 indicate rapid sedimentation. In contrast, the Fish Scale Formation in well 06-18-36-6W3 is comprised of abundant fish scale debris and horizontal burrows, which indicate that the western part of the study area was consistently within a deep water environment. 64 2.2.5 Belle Fourche Formation 2.2.5.1 Well 06-18-36-06W3 388.5-384.Om: shale, medium grey, platy to fissile, non calcareous; horizontal burrows. 384.0-382.5m: shale and siltstone interbedded; shale: medium grey, fissile, slightly silty; siltstone; light grey, non calcareous, horizontal burrows. 382.5-380.5m: shale: medium grey, non calcareous, fissile. 380.5-379.2m: shale and siltstone interbedded; siltstone, light grey, non calcareous, horizontal burrows, glauconitic in top portion; shale, medium grey, fissile, trace horizontal burrows. 379.2-375.Om: shale, medium to dark grey, platy to fissile, non calcareous, fragments of fish scales, bones; horizontal burrows, pyrite nodules. 375.0-372.Om: shale, medium grey, platy to fissile, non calcareous; few fish scale fragments, slightly horizontal burrows. 2.2.5.2 Well 03-28-33-23W2 350.2-350.15m: siltstone, light green, glauconitic, small-scale cross bedding (Fig 2.24). 350.15-350m: shale, dark grey, non calcareous. 350.0-349.95m: bentonite, cream white, sandy. 349.95-343.2m: shale, dark grey, blocky, non calcareous. 343.2-343.15m: bentonite, light blue, ashes. 65 f »»*«^Ji>< v\ I I Fig 2.24 Core photo of the Belle Fourche Formation in well 3-28-33-23W2 showing light green, glauconitic, cross bedded siltstone (350.2m). 66 343.15-340.8m: shale and sandstone interbedded; shale: dark grey, non calcareous; sandstone: light grey, very fine grained, thin layers, well sorted, less cements. 340.8-338.6m: shale, dark grey, blocky, noncalcareous. Interpretation The Belle Fourche Formation represents the second regressive pulse of the Colorado Group. In south-central Saskatchewan, the predominating dark to medium shale interbedded with thin siltstone beds indicates deposition in a offshore environment (Fig 2.22). The several thin beds of glauconitic cross bedded siltstone in the well 06-18-36-06W3 indicate increasing detrital inputs and storm influences. The well 03-28-33-23W2 to the east contains several sandy bentonite beds, which may be correlated to the X bentonite beds exposed in the Belle Fourche outcrop at the Bainbridge River (Schroder-Adams etal., 2001) 2.2.6 Second White Specks Formation 2.2.6.1 Well 06-18-36-6W3 372.0-368.0m: shale, grey, platy, highly calcareous with abundant white specks, interbedded with shell debris layers-Inoccramus (Fig 2.25A| 368.0-366.2m: shale, medium grey, platy, calcareous with a few white specks. 366.2-366.1m: bentonite, light grey. 366.1-363.2m: shale, dark grey, platy, highly calcareous with abundant white 67 1 CO 1 UJ 1 -< DC 1 ..taM r- J UJ 1 "^ i *» I I r,JWijflEg; Fig 2.25 Core photos of the Second White Specks Formation in well 6-18-36- 6W3. A. Abundant white specks, interbedded with shell debris layers- Inoceramus (370.5m). B. Shell debris layers-Inoceramus (360.7m); 68 specks; few fish scales, calcite strip and shell debris layer- Inoceramus on top portion. 363.2-349.6m: shale: medium grey, platy, highly calcareous with numerous white specks, interbedded with shell debris layers-Inoceramus (Fig 2.25B); a few fish scales. 2.2.6.2 Well 03-28-33-23W2 338.6-335.4m: interbedded shale, sandstone and bentonite; shale: dark grey, blocky to flaky, highly calcareous, abundant white specks and shell debris layers-Inoceramus; sandstone: light grey , noncalcareous, very fine to fine grained, cross bedded (Fig 2.26A), at the bottom contact surface; bentonite: light blue, blocky to fissile, 4 layers each with a thickness of 10-50cm. some well preserved fossil moulds (Fig 2.26B) 335.4-330.7m: shale, dark grey, blocky to flaky, abundant white specks, calcite strips in upper portion (Fig 2.26C) abundant white specks, calcite strips and shell debris-/nocerami/s, some pyrite concretions; bentonite: light blue, fissile, seven thin layers interbedded with shales. 327.6-319.2m: shale: dark grey, blocky to platy, highly calcareous with abundant white specks, visible crystals (Fig 2.26D), bioturbated, burrows filled by calcite; calcite strips in upper portion, thin layers rich in 330.7-327.6m: interbedded shale and bentonite; shale: dark grey, blocky, fossils 69 Fig 2.26 Core photos of the Second White Specks Formation in well 3-28-33- 23W2. A.cross bedded sandstone (338.6m); B. well preserved fossil mould (336.3m); C. calcite strips (.333.1m); D. White specks, visible crystals of calcite (327.6m) 70 in lower portion. Interpretation The Second White Specks marks the maximum transgression in the Late Cenomanian to Early Turonian (Kauffman and Caldwell, 1993). In the study area, the Second White Specks is interpreted to have been deposited in a lower offshore environment (Fig 2.22). In the eastern well 03-28-33-23W2, the basal contact with the underlying Belle Fourche Formation consists of interbedded layers of sandstone and bentonite that are rich in Inoceramus debris. In the western well 06-18-36-6W3, the deposits change from noncalcareous to highly calcareous shale. Persistent anoxic water conditions are indicated by the dark shale that is well laminated by calcareous white speckled layers and is without any bioturbation. The abundant Inoceramus debris, especially abundant in the upper portion, also indicates anoxic water conditions because Inoceramids are epifaunal suspension feeders, which are known to have been capable of surviving anoxic environmental conditions that were limiting factors for other species (Kauffman, 1988). The bentonite thin beds which are formed by volcanic ash decomposing represent the maximum flooding surfaces of peak transgression. 71 2.2.7 Carlile Formation 2.2.7.1 Well 06-18-36-6W3 349.6-347.6m: shale, medium grey, platy, noncalcareous, a few fish scales and bones. 347.6-340.5m: shale, light grey, platy, non calcareous; fragments of fish scales, bones; pyrite concretions, bentonitic on top. 2.2.7.2 Well 03-28-33-23W2 Not present. Interpretation In the eastern well 03-28-33-23W2, the noncalcareous Carlile shale is missing. In the western well 06-18-36-6W3, the 9m noncalcareous shale with abundant fragments of fish scales and bones is an erosional remnant of Carlile deposits. An important unconformity exists between the lower speckled zone (Second White Specks) and upper speckled zone (First White specks) that has been proved by Microfauna studies in central Saskatchewan (Price and Ball, 1971, 1973; North and Caldwell, 1975). The facts that Carlile is thin in the western well 6-18-36-6W3 and is missing in the eastern well 3-28-33-23W2 might be caused by this unconformity. It was likely deposited during regression of sea level and is interpreted as upper offshore environment (Fig 2.22). 72 2.2.8 First White Specks Formation 2.2.8.1 Well 06-18-36-6W3 340.5-336.2m: shale: light grey, platy, calcareous with white specks; fragments of fish scales and bones; pyrite nodules, ammonite and bacculite debris (Fig 2.27A.B). 2.2.8.2 Well 03-28-33-23W2 319.2-319.15m: shale: dark grey, blocky to platy, highly calcareous with abundant white specks. 319.15-315m: shale dark grey, blocky-flaky, highly calcareous with white specks 315.0-308.7m: shale and shell debris layers interbedded: shale: dark grey, blocky-platy, highly calcareous with abundant white specks, wood pieces (Fig 2.28A), and hummocky bedding in lower portion; shell debris (Inoceramus) layers (Fig 2.28B) -five thin layers (0.5-1.5cm) interbedded with shale. Interpretation The First White Specks Formation is characterized by thin and highly calcareous dark shale with abundant white specks. It represents the latest transgressive event of the Colorado Group and the dark to medium grey calcareous shale package is interpreted as deposited in an offshore environment (Fig 2.22). In the western well 06-18-36-6W3, it is separated from the Second 73 Fig 2.27 Core photos of the First White Specks Formation in well 6-18-36-6W3. A. Fragments of fish scales and bones, pyrite nodules (340.1m); B. Bacculite debris (338.5m). 74 Fig 2.28 Core photos of the First White Specks Formation in well 3-28-33-23W2. A. Wood pieces (313.2m); B. Shell debris (Inoceramus) layers (311.5m) 75 White Specks Formation by the thin non calcareous Carlile shale. However, in the eastern well 03-28-33-23W3, it sits directly above the Second White Specks, indicating an erosional unconformity. The hummocky stratification indicates storm influences. The big wood piece was likely transported offshore from the coast by this storm. 2.3 Montana Group 2.3.1 Milk River Formation 2.3.1.1 Well 06-18-36-6W3 336.2-333.Om: shale: light grey, platy, noncalcareous. 333.0-320.Om: shale, light grey, platy, abundant plant fragments; several sandy red shale layers interbedded with light grey shale, pyrite concrete, ammonite, bentonite layers on top. 320.0-314.5m: shale, light grey, platy, non calcareous, abundant plant fragments, sideritic, slightly bioturbated, few burrows; red sandy mudstone layer at base, sharp contact with underlying shale. 2.3.1.2 Well 03-28-33-23W2 308.7-308.68m: sandstone, green, very fine grained, non calcareous, bentonitic. 308.68-302.9m: shale, medium grey, blocky to flaky, non calcareous, abundant pyrite nodules, fish bone debris and burrows; wood pieces (Fig2.29). 76 Fig 2.29 Core photos of the Milk River Formation in well 3-28-33-23W2. A. Wood pieces (306m); B. Pyrite nodules (305.4m); C. Abundant fish bone debris (305m); D. Foot prints (297.9m) 77 302.9-297.Om: shale and numerous bentonite layers interbedded; shale: medium grey, blocky to flaky, non calcareous, abundant burrows, big foot prints (Fig 2.29); bentonite: cream, cream white, many thin layers (2-10cm) interbedded with shale. 297.0-286.4m: shale, dark grey, blocky, non calcareous, pyrite concretions and burrows, microfractures within upper part. Interpretation The Milk River Formation in study area is a different depositional system from the Milk River sandy deposits of southwestern Saskatchewan, which has been interpreted as a proximal shelf to offshore environment (Pedersen, 2003). The abundant plant fragments and red mudstone indicate a coastal setting and subaerial exposure, and the abundant burrows and bentonite beds likely indicate a well oxygenated open marine environment. It is likely deposited in a tidal muddy coastline environment in central Saskatchewan in which the sea level frequently fluctuated. 2.3.2 Lea Park Formation 2.3.2.1 Well 06-18-36-6W3 294.5-291.5m; shale, light grey, fissile, pyritic and sideritic; dark brownish grey, weathering to light yellow brown, calcareous ironstone concretions in upper portion; sandstone: light grey, very fine grained 78 crossbedded, argillaceous, sharp contact with underlying shale (Fig 2.30A).rhythmites in lower portion; crushed bacculites (Fig 2.30B), ferruginous, mud with chert grains; chert septarian nodules with calcite filled cracks at base, sharp contact. 291.5-278.Om: shale, light grey, silty, abundant sphaerosiderites, iron oxide bands; 278.0-277.5m: bentonite, muddy, brownish grey, fragmented. 277.5-272.Om: shale, light grey, blocky to fissile, silty, sphaerosiderite concretions, rhythmites, base sharp contact by chert septarian nodules, cleavages and joints filled by calcite (Fig 2.30C). 272.0-258.Om: shale, light grey, blocky to flaky, silty, sphaerosiderite concretions, ferruginous strip; seasonal laminae; base sharp contact by 10cm oxidized mudstone interbedded with chert septarian nodules with cracks filled by calcite (Fig 2.30D). 258.0-257.5m: bentonite, light grey brown, muddy; broken into pieces. 257.5-242.3m; shale, light grey, silty, sideritic, sphaerosideritic concretions; ferruginous strip, seasonal laminae, slightly bioturbated, few crushed baccutites. 242.3-221.2m: shale: light grey, blockly to flaky, silty, sideritic; some iron stains and ferruginous strips, seasonal laminaes; slightly bioturbated, intense upwards; some burrows filled by calcite. 221.2-167.Om: shale, light grey interbedded with 4 red mudstone thin layers; blocky to flaky, silty, sideritic, bioturbated, seasonal laminae, shell 79 Fig 2.30 Core photos of the Lea Park Formation in well 6-18-36-6W3. A.Unconformable contact with underlying shale (294.5m); B.Crushed bacculites (281.9m); C.Sphaerosiderite concretions, cleavages and joints filled by calcite (273.3m). D. chert septarian nodule with cracks filled by calcite (272m). 80 debris, crushed bacculites; sharp contact with underlying shale by 1cm fine grained sandstone. 167.0-169.9m: limestone, coarse crystals, organic rich, recrystalized in part. 169.9-165.3m: shale; light grey, silty, sideritic, bioturbated. 165.3-165.1 m: limestone, argillaceous, iron stained, synaeresis cracks filled by calcite at base. 165.1-145.3m: shale, light grey mudstone interbedded with 3 thin layers of red mudstones; blocky to flaky, silty, sideritic, bioturbated, a few shell debris and crushed bacculites. 145.3-142.0m: limestone, medium grey, argillaceous, fractures filled by calcite veins. 142.0-141.3m: limestone, medium grey, ferruginous. 141.3-129.7m: shale, light grey, silty, bioturbation intensifies upwards, rich in Terebelina, rare gastropods. 129.7-127.7m: sandstone, grey green, blocky, slightly argillaceous, very fine to fine grained, coarsening upwards, strong bioturbation, shell debris. 127.7-127.5m: limestone, light grey, ferruginous, argillaceous, fractured, fractures filled by calcite veins. 127.5-126.7m: sandstone, grey green, argillaceous, strongly bioturbated, very fine grained, coarsening upwards. 126.7-116.3m: shale, light grey, blocky, silty, sideritic, bioturbated, some plant fragments and shell debris. 116.3-116.2m: sandstone, light blue, very fine grained, bentonitic, crossbedded. 81 116.2-114.0m: shale, light grey, blocky, sideritic, bioturbated, some plant fragments. 2.3.2.2 Well 03-28-33-23W2 286.4-286.1 m: breccia, grey green, unconformable surface with underlying shale. 286.1-267.0m: missing core. 267.0-219.5m: interbedded shale and bentonite beds; shale: light grey, blocky, non calcareous, abundant burrows with some filled by pyrite, sandy and intensive bioturbation in top portion, small scale fault; bentonite: three thin layers, cream white. 219.5-180.0m: shale, light grey, blocky, non calcareous, sandy due to intensive bioturbation, abundant burrows filled by pyrite or sand; two thin layers (2cm thick) of very fine grained sandstones interfingering with thick blocky shale. Interpretation The Lea Park Formation represents the transgression of the Claggett marine cycle during Campanian time (Kyser etal., 1993). In central Saskatchewan, the lithology associations seem distinct from southwestern and southeastern Saskatchewan, where the Lea Park consists of dark marine shale intertonguing with the Belly River thin sand beds (Christopher and Yurkoswki, 2004). In the eastern well 03-28-33-23W2, the light grey shale with abundant burrows indicates an open shallow marine environment. However, in the western well 06- 18-36-6W3, in addition to the shallow marine shale deposits, several partly 82 oxygenated shale beds with sphaerosideritic concretions and red iron strips indicate subaerial exposures. The numerous chert septaria nodules between those shale beds likely formed syndepositionally or during early diagenesis as indicated by the lack of cross cutting with surrounding strata. All above evidence shows that the Lea Park Formation was deposited in a coastal to muddy shoreline environment. 2.3.3 Belly River Formation 2.3.3.1 Well 06-18-36-6W3 114.0-113.0m: mudstone, oxidized red mudstone interbedded with one layer of light grey mudstone. 113.0-111.3m: mudstone, light grey, fissile, sandy upwards. 111.3—109.8m: sandstone, light grey, fissile to blocky, very fine grained, loose, crossbedded. 109.8-102.8m: sandstone, light grey, red (oxidized), fissile, very fine grained; truncated with muddy beds, some plant fragments. 102.8-96.8m: mudstone, light grey, blocky, sandy, truncated with sandy bed (Fig. 2.31 A), some plant fragments. 96.8-77.4m: sandstone, seven fining upwards cycles, each cycle varying from very fine grained sandstone to siltstone; grey to green, loose, truncated beds, abundant plant fragments, rich in carbonaceous debris. 83 Fig 2.31 Core photos of the Belly River Formation in well 6-18-36-6W3. A. Muddy beds truncated with sandy beds (96.4m); B. Coaly mudstone with roots (73.1m) 84 77.4-74.9m: sandstone and mudstone interbedded; sandstone: light grey, loose, very fine grained, argillaceous, abundant carbonaceous debris; mudstone: light grey, fissile, sandy. 74.9-74.8m: mudstone, brown red, blocky, sandy, coaly. 74.8-67.Om: sandstone: grey green, loose, clean, very fine grained, well sorted, crossbedded, coal seam in upper portion (Fig 2.31 B). 67.0-56.5m: sandstone, grey green, blocky, loose, medium to very fine grained, three fining upwards cycles (Fig 2.32); from 59.1-58.5m, 0.6m calcareous fine grained sandstone with abundant plant fragments and carbonaceous debris. 56.5-55.4m; siltstone and mudstone; sandstone: lower portion, cream white, crossbedded; mudstone: upper portion, light grey, silty, coaly. Interpretation The Belly River Formation can be divided into two lithofacies associations (Fig 2.33). The lower lithofacies association is from 114-74.9m, and the upper lithofacies association ranges from 74.9-55.4m. The lower lithofacies association is interpreted as a tidal influenced fluvial to estuarine environment. The sandier upwards mudstone bed and crossbedded sandstone bed at the basal Belly River formed a coarsening upwards cycle and likely suggests estuarine mouth bar facies. The stacked inclined heterolithic stratifications represented by sandy beds truncated with muddy beds indicate bi-directional flow influence. The bi directional flow features, as well as abundant plant fragments, indicates a tidally 85 ~f. :•.-. •'•«>.tif' ! Fig 2.32 Core photos of the Belly River Formation in well 6-18-36-6W3. Photo shows Grey green, blocky, loose, medium to very fine grained sandstone (67- 56.5m) 86 O Tl ^CQ' W IV) Belly River Formation CO CO Lower lithofacies Upper lithofacies zr association association p 100 m — 90m - oT 110m - 80 m — 05 o o O CD" 3 3 7 - L m r-'^_C " Tida l influence d c/> .J _' / fluvia l t o estuarin e t •Mr i en C7) en 11 P o 1 Win 'I CO cu" J \ -—^ GO o' i r UI uJ C/3 f P IT CO CD 00 03 Q JJ < <' CD 03 p' P CD 00 1 CO 03 influenced fluvial system. The upper lithofacies association is interpreted as a fluvial environment. It is separated from the lower lithofacies association by a thin brownish coaly mudstone bed with rooting beneath. This coaly bed was formed in a flood plain facies. Above the coaly succession, the several medium fine to very fine grained fining upwards sandstone beds with cross bedding and carbonaceous debris represent typical fluvial channel deposits. 88 Chapter 3. Stratigraphic Correlation 3.1 Introduction In the previous chapter, lithologies and facies for each formation were described and analyzed in detail. This chapter will address their lateral variations by constructing a regional cross section from southwest Saskatchewan to southeast Saskatchewan, and some local cross sections in the study area. The lithofacies observed in the cores were integrated with wireline log features to correlate the stratigraphic variation and recognize unconformities. One regional cross section from southwestern Saskatchewan through the studied area to southeast Saskatchewan and three local cross sections in the study area (Fig 3.1) were built for this project. Three of them, including the regional and two local ones (A-A', B-B', D-D'), were tied to each other and to the two core-logged wells to keep consistency between the core divisions and wireline log correlations. The lithostratigraphic correlation method, which is the subdivision of the rocks based on the same or similar lithology that can be recognized over a wide area (Coe, 2003), is used in this study. The lithostratigraphic units are often diachronous and include, in descending order, formations, members and beds (Coe, 2003). The maximum flooding surface represented by the top of the Second White Specks was used as the correlation datum. Because most of the Cretaceous strata are dominated by marine shale deposits, with the exception of the Mannville continental to marginal marine deposits, the resistivity wireline log and gamma-ray log are likely the best tools 89 *8 %|iPt.wrti« 21 t«j %^.^|iiac2oua ^j *«+fit **&<*%* * tf R9 W RT RS fW m R2 fW RJ8 R2? R36 &2§ fg# K23 832 831 3|pj gfJ? *» '45 P& R/ ffj? fti1 ?-»8 R9 * If R? F& W K* Rj FP fW m& »/? pjg &$ * "*' »S • * - • s„ «* • • -,. ng ,-g + .• • < • £ . (•5 + ii» iS 4 • • • + • * Sw * T#< * + • * * "5 •- « *• f f3 • ' * * •. >s • / p x <* • * >«* • TS *• • « >- *3**~ ^fr / T~ V • » */ eiif % B"J 8 p»^- pt+ 4»» rS I! *• *y* ;>V*- •c * -"'»FV */7 • * * *» »V' n + • • i5r?« m * *t** * / *? a •; *- * S'" T 1 T 2 * \l »v~« * * ° * + * ! | < » 1 * ** * ' !•!*" g + * / + * • \ 4 f * ^ * p J / 4- TV *+ • E t*# it** • * 5 2 88 S3 ' m *R P& m *3 »2 21 fi^l * RI; J??E si? R?4 ; s^ R3» j5 * * P''i r$- » * r* T1U me «8 Re R? ras R9 m P3 R2 vm R2S R37 SM &2* RS R2 2SW3 "•SSLJ Fig 3.1 Map of studied area showing the cross sections. 90 for correlations. The borehole is generally irregular in shale intervals and thus affects the accuracy of density logs. In this study, both gamma-ray log and resistivity log are used for the regional cross section. However, in the study area, most of the available resistivity logs are Elogs that were logged during 1950s- 1970s and have low resolution. Thus for the local cross sections, Elogs were only used in cross section B-B' for supplementary comparison. Gamma-ray and density logs are used in C-C and D-D'. The four constructed cross sections in this study are shown in Fig 3.2, Fig 3.3, Fig 3.4 and Fig 3.5. A cross section of the Mannville Group E-E' (Fig 3.6) tied in the studied core well (6-18-36-6W3) was modified from previous work (Christopher, 2003) and used as a reference of Mannville Group correlation. 3.2 Structure and Isopach maps Structure maps for 2 key surfaces, the top of the Mannville Group and top of the Colorado Group (Fig 3.7, Fig 3.8), and an isopach map for the Colorado Group (Fig 3.9) were created for central Saskatchewan. The data used for mapping was retrieved from well tickets in GeoScout. The data quality was checked during mapping and unreasonable data has been corrected by reference to logs or deleted (no logs).The purpose of these maps is to show the current structures and overall thickness trend for the Mannville and Colorado Groups to guide the stratigraphic correlations. The thickness for each discussed 91 10-29-26-22W3 06-20-28-18W3 16-04-024-27W3 GR Res GR Res 10-24-32-17W3 07-33-24-25W3 GR _.. Res 13-15-31- GR Re Fig 3.2 Regional Cross A-A' from southwestern S< A' Core Core (6-18-36-6W3) (3-28-33-23W2) B-B' D4)' W3 13-07-36-6W3 04-28-33-23W2 06-22-15-33W1 01-02-21-31W1 GR DNPS a>6» I •oil 1 "N •% J?« ,, I \ 1 ikatchewan through central to southeastern Saskatchewan KS< v \ \» 1 ^ kl' **'"* \ All tJt fP" Regina \ / Is •am, KJ> Moose Jaw * V* Kp • *$k ? •h •^BBBK^kSaX- 1 »* * _LJE1KJ )2 B Core (6-18-36-6W3) A-A' 13-7-36-6W3 16-26-36-4W3 -34-35-3W3 16-11-34-2W3 13-22-34- Fig 3.3 West-east cross se< B' Core (3-28-33-23W2) 16-33-33-28W2 10-22-33-27W3 4-29-33-26W2 13-19-33-25W2 6-29-33-24W2 13-34-33-23W2 W*«l"V.w*». A j«**KXh**i«l 'J *- •*« * **#«"«• c-1 tat *i K4 M m IM BJ M I»I ret ea nI SS' "' " *» KM mm « 2IS * B B S s- • ", « * • «s •* t -» • • « • » 5* * ? . t* 4 • ;- #i » 8« *« • section B-B' through the study area *• *> *-. * * ••.. e fn i*i *> , k • *; 1^ _ !*' • f . • n1' '. 2 - ; 1' • * * t - 1 , E •* ' i s- * ! ••" T,i V * ,8 =S- r• « ^- • £ E e # , • <\ t * *•€ '* ,. c " *• .* r* . / • *wr f 1 - • I.* y* ' 4 " *# • **i *'- e 5 *c V . •TJ * 5, * s NW >S to . ft* « m WJ M1 « u (QJ B» 1IW *•* M 93 6-15-31-4W3 4-29-33-2W3 6-27-32-1W3 13-22-34-1W3 I Fig 3.4 Cross Section C 94 c 12-12-38-28W2 16-6-39-27W2 Lea Park Milk River First White Specks Second White Specks Belle Fourche Fish scale (Westgate Viking llilo Fou LI Mannville »*"• i • •a«\«kf"M)%i ""il * •*- a ,**.**•*#> 0>] m r M HI m Bf j» 81 82 i«9 JBM RM BM BIS S3* ns tea m» uptfe 2*ffi «. ». .. » !» » - . ^ ««• * ** «S " - .- - $* R • ** » ' : * ra» r-^r-r-P" » • * » r-U-Ll ••I* Br * •• * Jt ,•• . ' •• LJ S" .»• 2 • * ** r •fe • • .•« it • r •14 J Pi, rft w • pN ft- ». 1 ,P .. ., }fi4-»* ~t ui ?f i" "r P V> r v> h B • " * V 3 f * %T'-' B "» >* _2£* V-':» (^ t . * > / T •• ',' V> •"..'« e. •• v' /' * ^ "^'r-^* Pwt ™ «. «P » w * « fvift '' *«* e A j, ,*•(».: M ^1 E=, * - •» ^J • "» C» * t as w RJ M as M R3 Fig 3.5 Cross Section 95 D' 16-25-33-23W2 » 15-14-40-20W2 -iii- %^z HJ F" A. ^a'jrlsifrs r ' —- www •" HM' tCNMi — ~ • - - ... *™Z~*-JZ Lea Park Milk River First White Specks Second White Specks Belle Fourche Fish scale Westgate Viking Jilo Fou Mannville 3 •#•-•« «v i» <* *«] as M JO- Rl RS R* r S3 . B2 rii«7 . -tat S» RJi Ra* «3 *33 •" ]*« B ™ * • »> R. w » R> S» "» '» m .. - L.» i-j. •* <: • • ' ., * ' ™ & »T» ** ^ • >1 T, * + (!n .f • • » T3 • ** , *t • «* / * • • / S- >t *• •1S • .*» ' « * / » * * / rfj PI JS±. ^ B,sv ik -^ -W- A -**- V> -*"«- „* « FP1 tl -«* g™ • . . * '.ft* ' * > Brt g».» r.»• %r • * ' S.i\ * # L, J • • T< •tu. »' • . • ' •» .* ;1 '. *c' .* * * •. • • 1 •* fc" *• r* * . fv * v£ 4 Bm« *R R3»* R » » w „ „ AA '" ». ft! •* '<«* ». \» a L • B™ V • •.•v * * *s 1*L B mo no R. R7 R. RS R* R3 R2 1W3 RM Hi? R» KM R34 tai Z1W E CORE iabnyad GeotogicalSmey Report 223 FKJUB 15 - Southwest to northeast stratigraphic cross-section A3 - A31, cental Saskatchewan (From Christopher, 2003) Fig 3.6 Cross section E- E'of the Ma E' Mannville Group «r _ 96 ,T •( -. Q B R 25 R 22 R 21 R 2D R 19 R 1•- n 5¥^~1—L'-41^ jem •"-•F 'SO . " '' EsafSBBi^iiap' r •tat ;,'apnHaMiR( TM | J I \ I ' R 24 R 23 R 22 R 21 R 20 R 19—*»* W3M , at2M I RP HANATIA FNFRfY mUPANV I Fig 3.7 Structure map of the Mannville Group in the study area. Note: blue color represents structural highs and yellow represents structural lows. 97 Fig 3.8 structure map of Colorado Group in the study area. Note: blue color represents structural highs and yellow represents structural lows. 98 f — 1———, — , R 7 R 6 R 5 R * R 3 R 2 R 1 R 2B R 27 R 26 H 25 R 24 R 23 R 22 R 21 R 20 R 19 R 1- ^KSBBBBBBSHiBBR^^sir. T?' M R 24 R 23 R 22 R 21 R 20 R 19—U Fig 3.9 Isopach map of the Colorado Group in the study area. Note: the blue represents thickness greater than 160m and yellow represents thickness less than 160m. 99 formation from several researchers, including Marsh and Heinemann (2005), Christopher and Yurkowski (2004), and Pedersen (2004) are integrated with the stratigraphic correlation in this study. 3.3 Stratigraphic correlation 3.3.1 Mannville Group The structure map of Mannville Group shows an updip trend from southwest to northeast in the studied area (Fig 3.7) with a topographic relief of 300m. Two nose-like structures are developed in the west and southeast of the study area. 3.3.1.1 Cantuar Formation The Cantuar Formation in the study area is informally subdivided into 2-3 lithofacies associations. The lower lithofacies association is the transition zone from subaerial to subaqueous delta plain and is only present in the western core of the study area. It is characterized by several stacked cross-bedded distributary channel sandstones in the lower portion and intensively bioturbated interbedded sandstone and dark shale in the upper portion. The gamma-ray pattern is jagged to irregular with low API values in the sandstones and relatively high values in the shales. The overall trend of the gamma-ray is fining-upwards and appears as a bell-shaped log feature. The resistivity log trend is similar to the gamma-ray log and has a relatively even pattern (Fig 3.2, Fig 3.6). The basal unconformity is 100 easy to detect by dramatic changes on both gamma-ray and resistivity logs (Fig 3.2, Fig 3.3, and Fig 3.6). The increase or decrease in values across the boundary are laterally varied and depend upon the subcrop lithologies (Fig 3.6). The middle lithofacies association varies from fluvial to deltaic environments from east to west in the study area. The fluvial deposition is characterized by three upward-fining point bar sandstones separated by interfluve mudstones. The deltaic deposition is characterized by distributary channel sandstones interbedded with flood plain shale. The upper lithofacies association is a delta plain deposit. The deposits consist of five fining-upwards distributary channel deposits, with each channel sand overlain by inter-distributary shale deposits. In well 6-18-36-6W3, a coarsening upwards succession between the third and fourth fining-upwards cycles is interpreted as distributary mouth bar deposits. The middle lithofacies and upper lithofacies associations have log features similar to the lower lithofacies association, except that in the upper lithofacies the gamma-ray has funnel-shape intervals of mouth bar features interbedded with the bell-shape packages (Fig 3.6). The log pattern of the Cantaur Formation is an elongated funnel-shaped log trend with jagged gamma-ray and relatively even resistivity features (Fig 3.2, Fig 3.6). The Cantuar Formation is 57-87m thick in the studied area. It is thinning to the east and northeast with the increasing height of the Mannville structure (Fig 3.7). From the regional correlation, the Cantuar Formation fills and covers the pre-Cretaceous relief and significantly varies in thickness (Fig 3.2). 101 3.3.1.2 Pense Formation The marine Pense Formation overlies the Cantuar Formation on a relatively flat, planar disconformity (Christopher, 2003). The Pense Formation is less than 15m thick in the studied cores. It is characterized by fissile dark shale with interbedded calcareous sandstone (6-18-36-6W3) or siltstone and mudstone (3-28-33-23W2). The sediments are intensely bioturbated in both wells. In the study area, gamma-ray logs of the Pense Formation show funnel-shape patterns, while the resistivity log has an even appearance (Fig 3.2, Fig 3.6). The basal boundary with underlying Cantaur Formation is picked at the high peaks of both gamma-ray and resistivity logs. Regionally, the gamma-ray log patterns of the Pense Formation change from one funnel-shape pattern to several stacked funnel-shape patterns to the southwest and east Saskatchewan (Fig 3.2). The Pense Formation is persistently present over the geographic extent of the Mannville in Saskatchewan (Christopher, 2003) with thickness ranging from 45m thick in Southwest Saskatchewan to 15m thick in central Saskatchewan, and thickening to 20m to the east (Fig 3.2) 3.3.2 Colorado Group The structure of Colorado Group (Fig 3.8) shows the same trend as the Mannville Group. The thickness of the Colorado Group thins from southwest to northeast within study area ranging from 200m in the southwest to 120m in the northeast. The Lower Colorado Group is divided into two parts. The lower part was deposited during Late Albian to Cenomanian time, a period of about 12 102 million years, and consists of the Joli Fou, Viking, Westgate, Fish Scale and Belle Fourche Formations. The Upper Colorado Group consists of the Second White Specks, Carlile and Niobrara formations. 3.3.2.1 Joli Fou Formation The Albian Joli Fou Formation unconformably overlies the Mannville group (Christopher, 2003). In Central Saskatchewan, the Joli Fou Formation is comprised of olive to dark grey marine shale with abundant trace fossils and some pyritic concretions. Glauconite is common within the lower portion of the Joli Fou Formation. The lower boundary is placed at the top of the Pense Formation prograding sandstones or siltstones. The log pattern characterized by high gamma-ray values and low resistivity values with a box-shape is distinct from the underlying Mannville Group and overlying Viking Formation, and is recognizable in most of the region (Fig 3.2, Fig 3.3). The base boundary is picked at the point where gamma-ray increases and resistivity decreases. The gamma- ray has a relatively low value in the lower glauconitic silty portion that is identified as the Spinny Hill sandstone. The Joli Fou Formation is about 32-35m thick in the study area. The regional cross section indicates it is gradually thickening to southwest and southeast Saskatchewan (Fig 3.2). The log correlations also suggest an unconformity between the Joli Fou Formation and the Mannville Group. 3.3.2.2 Viking Formation 103 The Albian Viking Formation is used to designate the widespread marine sandstone above the Joli Fou Formation (Leckie et. al., 1994). Its distribution is discontinuous from one locality to another, with Viking sand bodies vertically occurring within a great shale package (Leckie et. al., 1994). In central Saskatchewan, the Viking Formation is comprised of light gray fine grained sandstones and thin siltstone beds within dark shale. A thin cherty conglomerate layer forms a sharp basal contact with the Joli Fou shale in the east logged well. The log pattern is characterized by jagged low gamma-ray and high resistivity in southwest Saskatchewan but laterally grades into one funnel-shaped peak in the study area (Fig 3.2, Fig 3.3, Fog 3.4, and Fig 3.5). The Viking Formation is 40 to 50m thick in southwest Saskatchewan and thins to 4 to 10m in central and eastern Saskatchewan. 3.3.2.3 Westgate Formation The Westgate Formation consists of grey marine shale with cross-bedded thin, very fine grained sandstone beds in the upper portion. The basal boundary is placed at the base of the thick shale overlying the Viking sand. The log pattern consists of high gamma-ray and low resistivity values and is generally even, with a few high peaks in both logs corresponding to transgressive flooding surfaces (Fig 3.2). The Westgate Formation is 100m to 70m thick in southwest Saskatchewan, thins to 28-35m in the studied area and thickens to 30-80m in southeast Saskatchewan. 104 3.3.2.4 Fish Scale Formation The Fish Scale Formation contains abundant fish remains (scales and skeletal material) within finely laminated, generally nonbioturbated sandstone and siltstone. Pebbles and nodular phosphorites occur locally. North and Caldwell (1975) noted that the faunas representing the early Cenomanian Stage associated with the Fish Scales Zone were missing in many parts of Saskatchewan and a regional disconformity likely exists between the Fish Scale Formation and Belle Fourche Formation. In the two logged wells of central Saskatchewan, the Fish Scale Formation is characterized by highly organic dark shale with abundant fish scale and fish bone fragments. The log pattern is characterized by irregular high gamma-ray and high resistivity and is easily picked in the southwest but becomes ambiguous in the study area (Fig 3.2, Fig 3.3). The thickness is 20m in the southwest and thins to 8-1 Om in the study area and in southeastern Saskatchewan. 3.3.2.5 Belle Fourche Formation In the study area, the Belle Fourche Formation consists of grey shale interbedded with shaly glauconitic siltstone in the lower portion and grey shale with fish scale debris in the upper portion. The well 03-28-33-23W2 to the east contains several sandy bentonite beds which may correlated to the X bentonite beds. The base boundary is picked on well logs at a decrease of both gamma- ray and resistivity reading. The log pattern shows two distinctive segments (Fig 3.2). The lower portion is defined by an even, low gamma-ray and low resistivity 105 trend, whereas the upper portion is characterized by a high gamma-ray and high resistivity log pattern. These two distinctive segments on the well logs become ambiguous in central Saskatchewan (fig 3.2, Fig 3.3), due to stratigraphic thinning out. The Belle Fourche Formation is about 20m in the southwest, thins to 7-17m in the study area and thickens to 25-15m to the southeast. 3.3.2.6 Second White Specks Based on foraminifera fauna, a study by North and Caldwell (1975) proposed that the Favel (Second White Specks) Formation conformably overlies the uppermost Ashville beds (Belle Fourche Formation) in Manitoba and eastern Saskatchewan. However, in west and central Saskatchewan, the Second White Specks Formation disconformably contacts with the underlying Belle Fourche Formation, which is proven by the absence of a fauna assemblage zone. The presence of this unconformity was also suggested by other workers (McNeil and Caldwell, 1981; Schroder-Adams etal., 1996). On the regional cross section and the local cross sections (Fig 3.2, Fig 3.3, Fig 3.4, Fig 3.5), the resistivity readings show consistently high values over a vast area due to its high calcareous content. The gamma-ray varied between high and low API values from place to place, but overall, changes from low to high values from south to central Saskatchewan. The gamma-ray features an irregular pattern, regardless of whether the reading is low or high. The thickness is generally uniform, but it is locally variable. In central Saskatchewan, it is 13-26 m thick. 106 3.3.2.7 Carlile Formation The Carlile Formation is comprised mainly of dark grey, non calcareous shale. In central Saskatchewan, the western well (6-18-36-6W3) contains 2m of Carlile shale, and it is absent from the eastern well. Seen on the regional cross section (Fig 3.2), the lower boundary between the Second White Specks Formation and Carlile Formation (where present) is easily recognized on well logs. In southeast Saskatchewan, the Carlile is characterized by an interval of abruptly high gamma-ray reading corresponding to the highly radioactive black shale, whereas in southwest Saskatchewan, the high gamma-ray interval is diminished to a surface boundary, which is also an abruptly high gamma-ray feature. The Carlile Formation above the high gamma-ray peak in southwest Saskatchewan shows an even to jagged log pattern with relatively low gamma- ray and resistivity values. The Carlile Formation is about 50m thick in the southwest and thins to 0-2m in central Saskatchewan, and thickens to 10m in southeast Saskatchewan. 3.3.2.8 Niobrara Formation The Niobrara Formation is about 150m thick in the southwest and thins to 20m in the study area and thickens to 100m to southeast Saskatchewan (Fig 3.2). It comprises three members; lower mudstone containing many thin bentonite layers (Govenlock Member), middle sandy portion (Medicine Hat Member) and upper calcareous speckled shale (First White Specks). On the regional cross section (Fig 3.2), the three members are easily identified on well logs in 107 southwestern Saskatchewan. The Govenlock Member has a jagged gamma-ray and even resistivity log pattern, and is separated from the underlying Carlile Formation by a high gamma-ray peak corresponding to a low resistivity peak. The Medicine Hat Member has the similar log pattern as the Govenlock Member, and the boundary is placed at the high gamma-ray and low resistivity peaks. The First White Specks has a log pattern of highly irregular gamma-ray and even resistivity trends. Towards the northeast, sandstones of the Medicine Hat pinch out and only two members can be recognized. As to central Saskatchewan, the wireline logs lose their distinct characters due to the Niobrara Formation thinning out (Fig 3.2, Fig 3.3) or pinching out in relation to the unconformity between Second White Specks and First White Specks, recognized by microfauna (Price and Ball, 1973; North and Caldwell, 1975). 3.3.3 Montana Group The Montana Group comprises the Milk River, Lea Park, Belly River and Bearpaw Formations. In the studied area, the Bearpaw Formation is missing. 3.3.3.1 Milk River Formation The thickness of the Milk River Formation ranges from 240-150m in southwest and west Saskatchewan to 23m-10m in central Saskatchewan, and thickens to about 50-100m in east and southeast Saskatchewan (Fig 3.2). The Milk River Formation consists of greenish bentonitic siltstone and shale in west and southwest Saskatchewan, and is more shaly in central and east 108 Saskatchewan. In west and southwest Saskatchewan, the log pattern is an elongate even trend on both gamma-ray and resistivity. The base boundary is picked at the point at which the highly calcareous shale turns to non calcareous bentonitic siltstone, and the gamma-ray values decrease significantly. The signature of the gamma-ray log remains low for the rest of the Milk River Formation (Fig 3.2, Fig 3.3). The upper boundary is the pre-Lea Park unconformity that is defined by recent studies (Christopher and Yurkowski, 2003). The log feature of the pre-Lea Park unconformity is distinctive by the abruptly lower gamma-ray and resistivity measurements, and is informally referred to as the Milk River Shoulder (Fig 3.2, Fig 3.3). The Milk River Shoulder is an important marker for the regional correlations. In central Saskatchewan, it is difficult to recognize the Milk River from cores due to the distal setting and the deep truncation by the pre-Lea Park unconformity, but the Milk River Shoulder still can be recognized on the logs. As the cross section extends into east and southeast Saskatchewan, the log signatures gradually shows its original characteristic Milk River lithology features. 3.3.3.2 Lea Park Formation The Lea Park Formation was deposited on a topography that was created by the pre- Lea Park unconformity. It fills the accommodation space left on top of Milk River Formation and the thicks and thins correspond to topographic lows and highs (Christopher and Yurkowski, 2003). The thickness of Lea Park Formation ranges from zero in northwest Saskatchewan to 180-260m in west to 109 central Saskatchewan (Marsh and Heinemann, 2005). In southeast Saskatchewan, the Lea Park thickness ranges 100 to 230m. The Lea Park Formation consists of thick grey to light grey mudstone with abundant plant fragments and burrows and fossils (Bacculite). Several subaerial exposure surfaces, indicated by iron oxide bands on mudstone, occur within the Lea Park Formation. The gamma-ray log pattern of Lea Park Formation is characterized by relatively low readings and an elongate jagged shape with many positive and negative peaks. The resistivity is relatively low and characterized by elongate jagged features with some very high peaks (Fig 3.2, Fig 3.3). The base of the unconformity is placed at the top of the Milk River Shoulder. The log signature of the top boundary is laterally varied and generally picked at the uppermost high peak of resistivity, corresponding to a low peak in the gamma-ray log in west and southwest Saskatchewan (fig 3.2). In central Saskatchewan, the top boundary is placed where the gamma-ray turns lower, reflecting the base of the Belly River thick sandstone (Fig 3.3, Fig 3.4, and Fig 3.5). 3.3.3.3 Belly River Formation The Belly River Formation is the uppermost stratigraphic unit that is below the surface casing and within the wireline log interval within the study area. The thickness of Belly River Formation ranges from 180-100m (Marsh and Heinemann, 2005) in southwest and west Saskatchewan to 50-80m in central Saskatchewan and 30-60m (Christopher and Yurkowski, 2004) in southeastern Saskatchewan. It is comprised of fine to very fine grained sandstone interbedded 110 with sandy mudstone with abundant carbonaceous fragments and some coal seams. In the studied area, the Belly River Formation is covered by the core of well 6-18-36-6W3, where the Belly River thickness is 56m. The gamma-ray log pattern shows a funnel-shape in west and southwest Saskatchewan and a varied to elongate box-shape in central Saskatchewan (Fig 3.2). This variation may be caused by vertical and lateral changes in the lithofacies packages. 3.4 Depositional environments and changes in relative sea-level The depositional environments are closely related to sea-level changes. Before continuing, it is necessary to define the types of sea-level changes. Eustatic sea-level refers to global sea-level and is the measure of the distance between sea surface and the centre of the earth. Relative sea-level is the distance between the sea surface and a local datum and is influenced not only by eustasy, but also by changes in the elevation of the continents and the sea floor. Water depth is the distance between sea surface and the top of the sediments (Coe, 2003). Based on the facies analysis and stratigraphic correlations, the sedimentary succession of the Cretaceous strata in central Saskatchewan was deposited in a variety of different depositional environments including continental fluvial, marginal marine delta, marine coastline, marine shoreface and offshore. The changes from one depositional system to another do not happen randomly and the different systems reflect the different combinations of accommodation space and sediment supply that are closely related to the relative sea-level 111 changes. In the studied area, there are three depositional systems that indicate the relative sea-level changes. Fluvial-deltaic system The fluvial-deltaic system formed during the deposition of the Cantuar to Pence Formations and corresponded to the First T-R cycle of Kauffman and Caldwell (1993). In vertical succession, the first relative sea-level rise is indicated by the depositional environment change from fluvial in the middle lithofacies to delta plain in the upper lithofacies in well 3-28-33-23W2, and from subaerial to subaqueous delta plain in the lower and middle lithofacies to delta front in the upper lithofacies in the well 6-18-36-6W3. The highest sea-level rise during this period is represented by the transgressive condensed deposits of the dark shale in the lower portion of the Pense Formation. The sea-level fall is indicated by the delta front coarsening upwards sandstone of the Pense Formation (Fig 2.9). Shelf system The shoreface to offshore of shelf system formed during Colorado depositional time (Fig 2.18 Fig 2.22). The Colorado is an overall marine shale package that was deposited during an overall eustatic sea-level rise punctuated by local, tectonically-induced relative sea-level drops (Schroder-Adams etal., 1996). Three T-R cycles that can be related to the T-R cycles defined by Kauffman and Caldwell (1993) were recognized in the study area based on core logging and regional correlations. The first is the Joli Fou to Viking T-R cycle 112 during which the environment changes from offshore to shoreface. The second is the Greenhorn cycle during Westgate to Carlile depositional time. The continuing offshore deposition from Westgate to Second White Specks represents the sea- level rise. The sea-level reached a maximum during the latest Cenomanian to early Turonian (Kauffman and Caldwell, 1993). This maximum sea-level rise is indicated by the lower offshore environment of the Second White Specks Formation. The regressive pulse of the Carlile Formation is not very obvious due to the unconformity between the Second White Specks and Carlile (where present) formations and the First White Specks Formation. In addition, there is a smaller order fluctuation of sea-level during Westgate to Belle Fourche depositional time with the sea-level fall is represented by the upper offshore environment of the Belle Fourche Formation. The third T-R cycle is the Niobrara Cycle during which time the Govenlock and First White Specks to Milk River Formations of the Montana Group were deposited. The offshore environment of the First White Specks Formation represents the latest sea-level rise of Colorado time. Coastline-fluvial system A fluvial to coastline system formed during the late Cretaceous and is represented by the deposition of the Milk River, Lea Park and Belly River Formations. The Milk River Formation is a tidal muddy coastline environment with occasional subaerial exposure and represents a relative sea-level fall during the Niobrara cycle. The thick succession of the Lea Park Formation is a 113 continuing muddy coastline environment above the Milk River Formation. The dark subaqueous shale deposits in the eastern, more seaward well 3-28-33- 23W2 may indicate relative sea-level rise. The tidally influenced fluvial to estuarine environment of the lower lithofacies to the fluvial channel environment of upper lithofacies in the Belly River Formation indicates that the relative sea- level dropped from higher to lower levels. 114 Chapter 4. Diagenetic Studies 4.1 Introduction This chapter presents the diagenetic studies of potential siliciclastic reservoir and source rocks of the Cretaceous strata in the study area, including petrographic characteristics and reservoir quality evaluation, Rock-Eval analysis of the source rocks potential, organic matter types, diagenetic stage, and stable isotope analysis of carbonate cements. The petrographic point counting, Rock- Eval analysis and stable isotope data are listed in Table 1, 2, and 3 respectively. 4.2 Petrography of sandstones 4.2.1 Compositions and textures A total of 90 thin sections taken from different rocks and formations within the two examined wells were observed with a petrographic microscope. Point counting (200 points) was carried out for 25 thin sections representing potential reservoir rocks (Table 1). Based on matrix content, sandstones are classified as arenites (matrix<15%), wackes (15% < matrix <75%), and mudstone (matrix>75%) by Dott (1964) (Fig 4.1). The arenites and wackes can be further subdivided by QFL (Quartz, Feldspar, and Lithic) plots (Folk, 1974). In the study area, 16 of 25 samples are arenites, while 9 of 25 samples are wackes (Table 1). The QFL plot of arenite sandstones (Fig 4.2A) identified 13 samples as quartzarenite, 3 samples as sublitharenite. The QFL plot of wacke sandstones 115 Table 1 Depth, porosity, and components of the sandstone samples from well 3- 28-33-23W2 and well 6-18-36-6W3 1 Depth Potosits Quail; Feldspar Lithic Claij Quart! Carbonate other TernanjQFL(x) 2 Sample Veil Formation Lithologj (m) pS\ (X) (X) (X) Hatiii(X) OBeigiowth(K) Cement'spi] (%) Quart! Feldspar Lithic J_ 04q»l03 6-18-36-6W3 Bella Riuer sandstone 69 11.5 20.00 10.00 29.50 15.00 0.5 7 0 33.6 16.8 49.6 _4_ 04qwl05 S-18-36-6W3 Belly River sandstone 73 10.5 3.00 7.50 40.00 1250 0 0 0 15.9 13.3 70.8 _5_ 03qw58 3-28-33-23W2 Viking sandstone 399 5.5 49.50 0.00 0.00 36.50 0 0 0 100.0 0.0 0.0 _6_ 03qw61 3-28-33-23W2 Joli Fou sandstone 401.8 18 23.00 0.00 10.50 43.50 0 0 2 68.7 0.0 31.3 _7_ 04q»52 6-18-36-6W3 Westgate sandstone 417 23.5 34.50 3.00 0.00 30.00 0 0 0 92.0 8.0 0.0 _8_ 03qw84 3-28-33-23V2 Cantuai sandstone 464.5 25 39.50 0.00 0.00 14.00 0 9 6.5 100.0 0.0 0.0 _9_ 03qw85 3-28-33-23V2 Cantuai sandstone 467.3 25.5 32.00 000 000 40.50 0 0 0 100.0 0.0 00 J0_ 04qw49 6-I8-36-SW3 Pense sandstone 483.5 4 58.00 0.06 1.50 24.50 0 12 0 97.5 0.0 25 It! 04qw46 S-18-36-SW3 Pense sandstone 485 0.5 52.50 0.00 150 8.50 0 35.5 0 97.2 0.0 28 1TJ 03qw33 6-18-36-6W3 Cantuar sandstone 493 46 45.50 0.0B 3.50 LOU 0 0 4 92.9 0.0 7.1 J3_ 04qw42 6-I8-36-6W3 Pense sandstone 494.4 22 46.00 0.00 0.00 8.00 0 27 0 1000 0.0 0.0 J4_ 04qw37 3-28-33-23V2 Cantuar sandstone 503 0 31.00 0.00 2.50 150 0 62 3 92.5 0.0 75 J5_ 03qw85 3-28-33-23V2 Cantuar sandstone 5032 37 60.50 0.50 100 0.00 0 0 1 87.6 0.8 16 J6_ 04qw31 6-I8-36-6W3 Cantuar sandstone 525 0 57.50 0.00 1.00 3.50 0 36.5 0.5 98.3 0.0 1.7 "iTi 04qw27 6-18-36-6W3 Cantuar sandstone 529.3 0 27.00 0.00 62.50 11.50 0 0 0 30.2 0.0 69.8 J8_ 04qw25 6-18-36-6W3 Cantuar sandstone 531 11 55.50 0.00 2.00 31.00 0 0 0 96.5 0.0 3.5 J9_ 04qw24 6-18-36-6V3 Cantuar sandstone 532.5 20 60.00 0.50 0.00 16:50 0 0 5.5 39.2 0.8 0.0 _20_ 04qw21 6-18-36-6W3 Cantuai sandstone 534.5 21.5 61.50 0.50 6.50 8.00 0 0 0 88.8 0.7 9.5 _2J_ 04qw14 6-18-36-6W3 Cantuar sandstone 545 0 32.50 4.50 11.00 45.00 0 0 3 67.7 9.4 22.3 J2_ 04q»10 6-18-36-6W3 Cantuar sandstone 552 4 55.50 0.00 0.00 15.00 0 0 . 25.5 100.0 0.0 0.0 J3| 04qw05 6-18-36-6W3 Cantuar sandstone 563 3.5 77.50 2.00 0X0 7.00 0 0 7 37.5 25 0.0 _24_ 04qw04 6-18-36-6W3 Cantuar sandstone 572 IS 70.50 100 &SS 4.50 0 0 tH 35.3 4.1 0.7 J5_ 04qw03 6-18-36-6V3 Cantuar sandstone 573.4 1 7i00 2.00 0.00 2.00 0 0 15.5 37.5 25 0.0 _26_ 04qw02 6-18-36-6W3 Cantuar sandstone 574.9 11 74<00 0.80 050 10.50 0.5 0 3 99.3 0.0 0.7 27 O4qw01 6-18-36-6W3 Cantuar sandstone 576 8.5 84.50 0.50 0.50 7.00 0 4 6 38.8 0.6 0.6 116 Table2 Rock-Eval analysis results of samples from well 3-28-33-23W2 Sample Depth (m) S1 S2 PI S3C02 Tmax Tpeak TOC HI OIRE6 FM 03qw01 185 8 0 03 0 28 011 0 73 429 469 0 73 38 88 03qw04 224 4 0 02 0 16 0 09 1 01 426 466 0 63 25 126 Lea Park 03qw06 244 5 0 01 0 12 0 08 0 93 435 475 0 65 18 117 03qw07 291 3 016 3 86 0 04 1 94 410 450 2 93 132 77 Milk River 03qw09 299 6 0 03 0 56 0 05 0 77 424 464 1 07 52 64 1st White 03qw10 305 4 0 12 2 82 0 04 1 34 400 440 2 28 124 61 Specks 03qw12 314 0 31 25 03 0 01 3 46 419 459 5 76 435 56 03qw14 320 0 20 20 76 0 01 2 49 418 458 4 45 467 54 03qw16 327 0 45 32 99 0 01 3 58 408 448 7 22 457 51 2nd White 03qw19 332 6 0 37 23 08 0 02 2 92 407 447 5 37 430 52 Specks- 03qw21 335 8 0 82 44 84 0 02 4 27 404 444 9 71 462 46 03qw27 340 2 0 55 19 04 0 03 4 00 398 438 6 94 274 58 03qw29 344 4 0 04 0 68 0 06 0 88 402 442 1 34 51 79 Belle 03qw30 346 4 0 02 0 67 0 02 0 87 418 458 1 42 47 60 Fourche 03qw33 351 7 0 04 1 57 0 03 0 68 418 458 1 58 99 42 03qw36 356 5 0 04 0 65 0 05 0 99 404 444 1 58 41 61 03qw38 363 6 0 03 1 94 0 01 0 83 433 473 1 72 113 51 03qw42 370 4 0 01 0 86 0 02 0 73 424 464 1 33 65 55 Fish 03qw44 372 0 02 0 70 0 02 0 88 420 460 1 39 50 69 Scale- 03qw49 379 0 04 1 15 0 04 1 46 410 450 2 07 56 79 Westgate 03qw50 383 0 01 0 43 0 03 0 55 419 459 1 02 42 44 03qw53 392 1 0 01 0 93 0 01 0 88 433 473 1 53 61 55 03qw56 398 8 0 02 0 95 0 02 0 71 429 469 1 31 73 50 03qw60 403 8 0 01 0 33 0 04 0 48 426 466 0 97 34 48 03qw63 408 9 0 00 018 0 02 0 38 431 471 0 73 25 56 03qw67 416 1 0 00 0 08 0 06 0 31 416 456 0 39 21 76 Joli Fou 03qw69 425 7 0 00 0 05 0 05 0 31 416 456 0 27 19 107 03qw71 433 5 0 01 017 0 06 0 43 428 468 0 92 18 36 03qw72 437 5 0 07 6 53 0 01 1 24 428 468 2 36 277 53 03qw74 444 7 0 03 3 09 0 01 1 26 432 472 218 142 55 Mannville 03qw75 446 5 0 07 2 84 0 03 1 17 432 472 1 91 149 52 117 Table3 Rock-Eval analysis results of samples from well 6-18-36-6W3 Sample Depth(m) S1 S2 S'2 PI S3C02 Tmax Tpeak TOC HI OIRE6 FM 04qw77 146 5 0 02 0 14 0 00 0 52 425 465 0 63 22 79 04qw76 165 2 0 03 1 23 0 00 0 02 0 86 359 399 0 82 150 85 04qw73 221 2 0 05 0 90 0 00 0 05 0 90 433 473 1 21 74 73 Lea Park 04qw72 248 4 0 02 0 55 0 00 0 03 1 04 435 475 1 25 44 77 04qw70 281 9 0 03 0 70 0 00 0 05 1 39 439 479 1 29 54 97 04qw68 314 2 0 03 0 60 0 00 0 04 0 69 423 463 1 22 49 55 Milk River 04qw67 325 011 1 26 0 00 0 08 0 64 424 464 1 41 89 44 1st White 04qw66 331 0 09 3 56 0 00 0 02 1 74 408 448 2 86 124 61 Specks 04qw65 335 2 0 32 7 72 0 00 0 04 1 24 418 458 2 97 260 43 04qw64 342 2 012 510 0 00 0 02 0 84 422 462 2 27 225 38 2nd White 04qw63 349 6 0 30 17 38 0 01 0 02 1 63 421 461 4 56 381 40 Specks 04qw62 363 2 0 29 1351 0 01 0 02 1 96 425 465 3 67 368 48 04qw61 373 0 22 5 42 0 00 0 04 0 99 408 448 2 65 205 39 04qw60 377 0 09 1 37 0 00 0 06 0 88 406 446 1 88 73 51 Belle Fourche 04qw59 382 0 24 0 81 0 00 0 23 0 73 405 445 1 47 55 51 04qw58 388 3 0 22 1 42 0 00 013 0 80 413 453 1 91 74 41 04qw57 390 5 012 0 85 0 00 012 0 83 415 455 1 65 52 54 04qw56 396 2 0 05 1 59 0 00 0 03 0 58 433 473 1 42 112 43 Fish Scale- 04qw55 401 2 0 07 1 37 0 00 0 05 0 57 434 474 1 38 99 37 Westgate 04qw54 404 2 0 07 1 31 0 00 0 05 0 65 421 461 1 48 89 38 04qw53 409 8 0 04 0 43 0 00 0 09 0 50 416 456 0 84 51 50 04qw51 472 0 02 012 0 00 013 0 90 425 465 0 56 21 121 Joli Fou 04qw50 480 019 0 87 0 00 018 0 95 422 462 2 00 44 44 Mannville 118 mudstones.. wackes_ arenites^ ^.quartz wacke ""arkosicj quartz wackej i. . = -. quartzarenite ~#J™, subarkose 5/\5sublitharenite. AJj&fX: t25 feldspathijrthi'cc Gtf^, percent matrix arkose tf^^hil ~. ££SM graywackei| < 3(V volcanic ;arkosic volcanic arenite •arsnite lithic ill : feldspar arenite*:- :> calclithite phyllarenite 50 rock fragments S 50 M sedimentary metamorphic Fig 4.1 Classification for sandstones (Dott, 1964) 119 Guaitt Quartzarenite Subarkose Sublitharenite Viking Pens* Westgate Cantuar Joli Fou Ee|/ River Feldspar Lithic Fig 4.2A Quartz-feldspar-lithic grain (QFL) diagram showing the composition of the framework grains of the arenite sandstones (after Folk, 1974) 120 Quartz wackes Subarkosic \ wackes \Sublithwackes Westgate Cantuai .Joli Fou BeSy Rivet Feldspai _7_— Lithic 25 50 Fig 4.2B Quartz-feldspar-lithic grain (QFL) diagram showing the composition of the framework grains of the wacke sandstones (after Folk, 1974) 121 (Fig 4.2B) identified 6 samples as subarkosic wackes, 1 sample as lithwackes, and 1 sample as feldspathic lithic wackes. The fluvial- deltaic sandstones of the Mannville Group contain an average of 55.0% quartz, 0.8% feldspar and 5.1% lithic fragments and the remaining 39.2% is comprised of 13.2% porosity and 26.0% matrix including clay, quartz, carbonate, other minerals (pyrite, mica, siderite) and organic or carbonaceous materials. Trace amounts of heavy minerals were also recognized. The Cantuar sandstone is generally moderately sorted and the shapes of the grains vary, ranging from sub-angular to sub-rounded. The marine sandstones of the Pense, Viking, Joli Fou and Westgate formations contain an average of 43.5% quartz, 0.6% feldspar and 2.7% lithic fragments. The remaining 53.2% is comprised of 10.3% porosity and 42.9% matrix, carbonate cements, and clay. These marine sandstones are well sorted and most of the grains have sub-rounded shapes. The Belly River sandstone is classified as litharenite and contains an average of 14.5% quartz, 8.7% feldspar and 34.8% lithic fragments, with much more lithic grains compared with the sandstones of the Mannville and Colorado groups. The remaining 42% is comprised of 11.0% porosity and 31.0% matrix, quartz overgrowth and carbonate cements. It is poorly sorted and most of the grains are sub-angularly shaped. In central Saskatchewan, the porosity of sandstones estimated from point counting ranges from 0% to 46%, with most samples in the range of 1% and 25% (Table 1). In the sandstones from the Cantuar Formation which account for 3A of the studied samples, the porosity shows a decreasing trend with depth (Fig 4.3). 122 4400 •'4-50 •-SB""-'* •v.: " "&**• '5 ' 550 600 • Cantaur( 6-18) Pense • Viking i westgate • Cantuar(3-28) Fig 4.3 Relationship between depth and porosity of sandstones from the study area. 123 The porosity trend of other sandstone formations is not clear due to scattered data points (Fig 4.3). 4.2.2 Diagenesis and paragenetic sequence Diagenetic processes in the Cretaceous in the study area include compaction, cementation, dissolution and replacement of framework grains and cements. The compaction is indicated by the types of grain contacts. Four major grain contact types- pointed, long, concavo-convex, and interlocked contacts are recognized in the studied sandstones. The long contacts and convex- concave contacts between quartz grains (Fig 4.4A) are common in the studied sandstones, suggesting a moderate degree of compaction. The presence of concavo-convex contacts and interlocked contacts between quartz grains indicates that the silica ions have been exchanged between quartz grains due to pressure dissolution (Fig 4.4B). Another indication of compaction is the deformation of ductile lithic fragments, matrix and micas. Cementation processes occurred between framework grains within the sandstones. Quartz, calcite, clay minerals and pyrite are the main cement types identified in the Cretaceous sandstones of the study area. The quartz cements commonly occur as overgrowths on the detrital quartz grains (Fig 4.5). The nonferrous calcite cement is distributed as patches and varied from 4% to as much as 36.5% in calcareous sandstones (Table 1). Two phases of calcite cements are observed. Phase 1 calcite cement completely occludes pore spaces and quartz grains appear to float within the calcite cement (poikilotopic 124 Fig 4.4 Photomicrographs showing petrographic features of sandstones of the Cantuar Formation from well 6-18-36W3. A. Long contacts (LC) and convex- concave (CC) contacts, 610.9m. B. Interlock contacts, 599m. 125 jfU9 Fig 4.5 Photomicrograph of sandstone from the Cantuar Formation of the Well 3- 28-33-23W2 (447.5m). Note the quartz overgrowth. 126 calcite) which has prevented compaction of framework grains (Fig 4.6A). This indicates that the phase 1 calcite cement precipitated before significant compaction and is the product of early diagenesis. This can be inferred by the fact that within a given thin section, the quartz grains are floating in calcite cement where there are calcites patches, whereas quartz grains are in contact with each other closely where there is no or little calcite cement (Fig 4.6B). In the areas of poikilotopic calcite (phase 1) patches, quartz overgrowths are seldom seen, indicating that the phase 1 calcite cements formed before quartz overgrowth. The phase 2 calcite cement is phaneric and only partly fills pore space (Fig 4.7A) leaving much open space, part of which could have resulted from later dissolution of previous calcite cements. In calcareous sandstones, where quartz overgrowths and phase 2 calcite coexist, the quartz overgrowths show irregular shapes and are overlain by calcite crystals (Fig 4.7B), demonstrating that phase 2 calcite cements were formed after quartz overgrowths. Calcite veins are found in the Lea Park Formation, filling the fractures in chert separian nodules (Fig 2.30D).The nonferron radial-fibrous calcite from the veins of separian nodules that formed syndepositional or early stage show well developed cleavage and undulatory extinction (Fig 4.8). Clay cements identified in the sandstone reservoir include chlorite and kaolinite. Chlorite occurs as a replacement of other clay minerals or coating framework grains. Quartz overgrowths were observed within the chlorite coatings, indicating the quartz overgrowths formed before chlorite authigenesis (Fig.4.9A). Kaolinite has alveolate features under the microscope and partly fills the open pores, and 127 Fig 4.6 Photomicrographs of sandstone of the Cantuar Formation from the well 6- 18-36W3. A. Phase 1 calcite cementation, quartz grains appear to float within the calcite cement (poikilotopic calcite) (561m); B.Precipitation of Phase 1 poiklotopic calcite occurred early in the diagenesis before significant compaction (496.1m); 128 ! *;?^.; *••* •..en ^s " *CC*£'S ¥^-'% ._ .J ^•'i- jaPta *S2SK8E>»»I,A .fc&Sk •'W&~'*~ "['M :tf/;flf€ ^ '^!v;iil Itr ife *'"' '• .. /,s; •S^"-- •'',^1 v' -,: l^^^^^f!,..-;.^ - Fig 4.7 Photomicrographs of sandstones of the Cantuar Formation from well 3- 28-33-23W2. A. Phase 2 calcite cememt, the edges of quartz grains show irregular shapes and overlain by calcite crystals (450.3m); B. The quartz overgrowths show irregular shapes and are overlain by phase 2 calcite crystals (450.0m). 129 v*^#*i^V-!; it ^'-W^W^,, M5»j«P^wvT*. -tffr^l; . -4-** ^<«n- Fig 4.8 Photomicrograph of nonferron radial-fibrous calcite from the Lea Park Formation of well 6-18-36-6W3 (145.3m). 130 ^m Fig 4.9 Photomicrographs of sandstone of the Cantuar (A) and Belly River (B) Formations from well 3-28-33-23W2 (A) and well 6-18-36-6W3 (B). A. Clay minerals chloritized and coated the quartz grains which are overlain by quartz overgrowths (467.5m). B. Belly River Sandstone with kaolinite postdating quartz overgrowth. 131 appears to have formed as the last diagenetic phase. In a few cases, kaolinite clearly postdates the quartz overgrowth (Fig 4.9B). In two samples of the Pense and Viking Formations, pyrite is the main cement and totally occlude the pore space (Fig 4.10 A, B). Siderite concretions were also observed in thin sections. Siderite occurs as sphericules with iron rims in the outer portion, which in some instances nucleate around existing quartz grains (Fig 4.11A). The coexistance of phase 1 calcite and siderite suggest they formed in the early diagenetic stage. In some shaly sandstones, the shale matrix and lithic grains were deformed by overburden compaction and form a pseudomatrix that played a significant role in the porosity reduction (Fig 4.11B). The processes of dissolution and replacement may have happened together. Thin section petrography shows that calcite remnants appear to float in the pores (Fig 4.12A), indicating that phase 1 calcite was dissolved afterwards. In some places, the calcite has irregular contacts with quartz grains and intrudes into the quartz, indicating that calcite replaced part of the quartz grain (Fig 4.12B). Dissolution of feldspar along the cleavage also occurred locally (Fig 4.13). Within the studied sandstones of the Mannville Group, volcanic and metamorphic rock fragments are present, especially within the basal sandstones (Fig 4.14A, B), and they provide important evidence for detrital source, as discussed in Chapter 5. Using the above petrographic observations, the paragenetic sequence of diagenetic minerals in the sandstones is summarized in Fig 4.15. There are two phases of calcite cements in which phase 1, poikilotopic calcite formed earlier 132 Fig 4.10 Photomicrographs of sandstones of the Pense Formation from Well 3- 28-33-23W2 (440.6m) (A) and Well 6-18-36-6W3 (483.4m)(B). 133 ,VXwr Fig 4.11 Photomicrograph of sandstone of the Cantuar Formation from well 3- 28-33-23W2 (A) and the Viking Formation from well 6-18-36-6W3 (B). A. authigenic siderite (463.2m); B. marine sandstone deposits were strongly winnowed and the textural maturity is high. Note the deformation of clay matrix (417.2m). 134 Fig 4.12 Photomicrographs of sandstone of the Cantuar Formation from well 6- 18-36-6W3. A. phase 1 calcite and dissolution (536.4m); B. calcite irregular contacts with quartz grains indicating that the calcite replaced part of the quartz grains (525.3m). 135 Fig 4.13 Photomicrographs of sandstone of Cantuar Formation from well 3-28- 33-23W23-28. Note feldspar Disolution (460.9m). 136 Fig 4.14 Photographs of sandstone of the middle lithofacies association of the Cantuar Formation in well 6-18-36-6W3. (A) volcanic fragments (V) (545.90 m); (B) metamorphic fragments (M) (545.90 m); 137 Phase 1 caJoite ceweiitttiaf ^^^^s? ^tanic^CQfaptfWrenii **#***»•• Siderite pr&cipiUtion . . ^^&r*s Qua i tz over gro ».-th " • • •••iwp*^— Pyrite precipitation ^^^mmm Phase J calcite cementation ^^™^™ Re.p:lacenfe.nt of calcite ^^^""^ Clay miiiera;! precipitat itfii -^—^— Fig 4.15 Paragenetic sequence of the Cretaceous sandstone reservoir in central Saskatchewan as established in this study. 138 and phase 2 calcite cements formed later, but no evidence of the two phases of calcite cements cut-crossing has been found. The dissolution of calcite cement and replacement of quartz overgrowths indicate that calcite dissolution and replacement happened after quartz overgrowths. In sample 04qw42 (495m), the relict calcite, dissolved from phase 1 calcite, appears to float in the pyrite, indicating that the pyrite formed after calcite dissolution. Clay minerals were the last diagenetic minerals precipitated in residual pores. Due to the long time span of the Cretaceous, this sequence is not always applicable for every sample and a specific phase did not occur at the same time. For instance, when the Belly River Formation was deposited, the Cantuar Formation might have already been subjected to significant burial diagenesis. 4.3 Organic matter study of shales In this section, the source rock potential and the thermal maturity of shale are studied. Interpretations of the data are based on the guidelines from Peters (1986) and Peters and Cassa (1994). 4.3.1 Rock-Eval analysis results The Rock-Eval analysis results are listed in Tables 2 and 3, and illustrated in Figs. 4.16, 4.19,4.22, and 4.23. Figure 4.16 and Tables 2 and 3 show Total Organic Carbon (TOC) variations with burial depth of wells 3-28-33-23W2 and 6- 18-36-6W3. The summarized Rock-Eval analysis for each formation is listed in Table 4. The TOC values can be divided into three groups (Fig 4.16, Table2, 139 Table3). The first group, represented by the Second White Specks shale and the First White Specks shale, are rich in organic matter, with the TOC values ranging from 1.22% to 9.71%. The 2 samples from First White Specks yield TOC values of 2.28-2.86%, with an average value of 2.57%. The 11 samples from Second White Specks have TOC values ranging from 1.22-9.71%, with a mean value of 5.05%. The second TOC group ranges from 0.63% - 2.07% TOC, and is mainly represented by the Milk River shale, the Westgate to Fish Scale shale, the Belle Fourche dark shale, the Mannville shale and the Lea Park shale of the western well 6-18-36-6W3. The 4 samples from the Milk River yield TOC values ranging from 1.07% to 2.93%, with an average value of 1.66%. The 15 samples from the Westgate to Fish Scale yield TOC values ranging from 0.84% to 2.07%, with an average value of 1.48%. The 4 samples from the Belle Fourche have TOC values ranging from 1.34 to 1.88%, with an average value of 1.53%. The 4 samples from the Mannville Group yields a TOC range of 1.42-2%, with an average value of 1.03%. The 5 samples from the Lea Park shale from the 6-18- 36-6W3 well yield TOC values ranging from 0.63 to 1.29% (Table 3), with an average value of 1.04%. The third TOC group contains samples with TOC values below 1 %, which are mainly from the Joli Fou shale and Lea Park shale of the eastern well 3-28-33-23W2. The 7 samples from the Joli Fou shale yield TOC values ranging from 0.27 to 2.36%, with an average value of 0.9%. The Lea Park shale of the eastern well 3-28-33-23W2 has TOC values ranging from 0.63 to 0.73% (Table 2), with an average value of 0.7%. The HI (Hydrogen Index) and Ol (Oxygen Index) for the Second White 140 Depth Vs. TOC of 6-18-36-6W3 Depth Vs. TOC of 3-28-33-23W2 T0C(%) TOC(0o) 0.0 2.0 4.0 6.0 8.0 10.0 DU : 0 1 Tl 0 150 \ 200^ *> ? 250 •=250 . < i Q. V Q Lea Park < i a. « Milk Ri\er 300 - <1 . li *C 2" WS-1" \VS 350 - 350- .«*" liciic iiuiivne 400 - f Westjulc-MS "150 J Joli lou '•-• Mannville \1ann\ille 450 500 - Fig 4.16 Plot of TOC versus Depth for wells 6-18-36-6W3 and 3-28-33-23W2 141 Specks-Carlile are 124-467mg HC/g OC and 38-61 mg C02/g OC, and are 124mg HC/g OC and 61 mg C02/g OC for the First White Specks (Table 4). The Westgate-Fish Scale and Milk River Formations have the same range of Ol (37- 79 mg C02/g OC and 44-77 mg C02/g OC respectively) but lower HI (41-113mg HC/g OC and 52-132mg HC/g OC respectively) compared to those of the Second White Specks-First White Specks formations (Table 4). The Joli Fou, Belle Fourche and Lea Park shales have very low HI values of 18-51mg C02/g OC (except one HI value of 277mg C02/g OC) and a big range of Ol (36-126mg C02/g OC). The 3 samples from the Mannville Group have HI values of 44- 149mg HC/g OC and Ol values of 44-55mg C02/g OC (Table4). 4.3.2 Source rock potential The quantity of organic matter generally can be measured by TOC values, but if TOC is less than 0.3 wt%, then all the related parameters are questionable and there is no hydrocarbon potential (Issler et al., 2005). Based on Peters and Cassa's (1994) criteria of evaluating source rock potential, TOC values ranging from 0.5-1.0 % indicate a fair source rock generative potential, TOC values ranging froml .0%-2.0 wt% represent a good generative potential, TOC value ranging from 2-4 % indicate a very good generative potential and TOC value greater than 4 % indicate an excellent generative potential (Table 5). In this study, the average values of the two sampled wells are used to evaluate the source rocks in central Saskatchewan. Table 4 is a summary of source rock potential for each formation. The results indicate that most of the Cretaceous 142 Table 4 Summary of Rock-Eval data from core samples of well 6-18-36-6W3 and 3-28-33-23W2 FM Tmax TOC HI Ol Kerogen Source rock Thermal (No of samples) (Degree) (Wt %) (mg/g) (mg/g) type potential Maturation Lea Park(7) 359-439 0 63-1 29 18-74 73-126 Type III fair- good immature Milk River(4) 400-425 1 07-1 67 52-132 44-77 Type III good immature 1s,ws(2) 418-419 2 28-2 68 124 61 Type II very good immature 2naws(11) 404-425 1 22-9 71 124-467 38-61 Type II/ III excellent immature Belle Fourche(4) 402-418 1 34-1 88 47-73 51-79 Type III good immature Fish Scale- 403-434 0 84-2 07 41-113 37-79 Type III good immature Westgate(15) Joh Fou (7) 416-431 0 27-2 36 18-277 36-121 Type III Fair immature Mannville(4) 422-432 1 42-2 0 44-149 44-55 Type III good immature 143 Table 5. Hydrocarbon source rock evaluation parameters for Rock-Eval pyrolysis data (modified from Peter and Cassa, 1994) Organic Matter Petroleum TOC Rock-Eval Pyrolysis Potential S1 S2 Poor 005 0O.5 02.5 Fair 0.5-1 0.5-1 255 Good 1-2 1-2 5-10 Very good 24 24 10-23 Excellent ^=4 ::=4 >2D Maturation Stage of Thermal Vitrinite Reflectance Rock-Eval Tmax Maturity for Oil Ro (%) rc) Immature 0.2-0.6 •5435 Mature Early 0.6-0.65 435-445 Peak 0.65-0 9 445-450 Late 0.9-1 35 450-470 Postmature >1.35 >470 144 shales in central Saskatchewan are good to excellent source-rocks (Table 4). The first group has average TOC values of 2.57% (First White Specks) and 5.05% (Second White Specks) indicating very good to excellent source rock potential. The second group has an average TOC value between 1 % and 2 %, indicating good source rock potential. The third group yield an average TOC value in the range of 0.5-1 %, indicating fair source rock potential (Table 4). The type of organic matter is very important in evaluating source rock quality and has a significant influence on the nature of hydrocarbon products (Peters, 1986). Organic matter types can be divided into 4 members that were derived from 4 different biological/chemical systems. Most of the organic matter occurred in a mixture of two or more organic matter types in varying proportions (Snowdon, 1989). The types of organic matter are essentially defined by the proportion of hydrogen bound in the organic structure (Snowdon, 1989). The most classic classification scheme is that of Tissot and Welte (1989), plotted as atomic ratios of O/C versus H/C (Fig 4.17). Espitalie et al (1977) pointed out that the hydrogen index HI and oxygen index Ol are proportional to the atomic H/C and O/C ratios, thus Ol versus HI cross plots can be used as an indicator of organic matter-kerogen types and their products. The cross plots of HI versus Ol of the two wells in central Saskatchewan are shown on Fig.4.18. The organic matter of the Second White Specks to Carlile shale has a mixture of Type II and Type III kerogen, which is Oil/Gas prone (Tissot and Welte, 1989). All the other shales fall into the Type III area, which is gas prone. 145 Principol products of kerogen evolution C02,B20 030 Oil »- Atomic O/C 60s 4.17 Van Krevelen diagram showing kerogen paths and products of maturation (from Tissot and Welte, 1989). 146 HI vs. 01 of well 3-28-33-23W2 HI vs. 01 of well 6-18-36-6W3 • i... ",•- •;M-IA- &.-.r-~i:'.<. • :.-•. i*-t • .--•a-.-.; aur-.i-.h x .-. .'•! ite Fish Scale X JolivFou • Mannville x •*• •'•''*'••• r:- U A x :.•• .IV. • M.M . :.• Fig 4.18 Plot of H/C vs. O/C of shale samples from well 3-28-33-23W2 and well 6-18-36-6W3 147 4.3.3 Thermal maturity Several parameters obtained from Rock-Eval can be used as organic matter maturity indicators. Rock-Eval Tmax increases progressively with thermal maturity and is controlled by the type of organic matter and the mineral matrix. Tissot and Welte (1989) proposed that Tmax is a good maturity indicator between 420°C and 460°C in Type II kerogen and between 400°C and 600°C in continental-derived Type III kerogen. In this study, Peter's (1986) criteria of a Tmax of 435°C as the limit between immature and mature of organic matter is used. Production index indicates the amount of in situ hydrocarbon generation as a function of thermal maturity and organic type and richness (Issler etal., 2005) Almost all samples have a Tmax below 435°C (Fig 4.19, Table 2, 3), indicating that the organic matter is immature in central Saskatchewan (Table 4). Organic matter thermal maturity is closely related to the diagenetic stage. The diagenesis of organic matter is of importance in understanding the generation and migration of oil and gas, and in evaluating the source rock and its level of maturation (Barnes et al. 1990). There are three stages of organic diagenesis: diagenesis, catagenesis and metagenesis (Tissot and Welte, 1989). In order to prevent confusion between reservoir diagenesis and organic diagenesis, the diagenetic classification scheme of Choquette and Pray (1970) is used here (Fig.4.20). The diagenesis stages of eogenesis, catagenesis (oil) and metagenesis (thermal gas) can be defined using the optical properties of source rocks (vitrinite reflectance~Ro). The standards are as follows (Tissot and Welte, 1989): 148 Depth Vs. Tmx of 6-18-36-6W3 Tmx(°C) 350 360 370 380 390 400 410 420 430 440 450 ;.iiiK*v '50 100 200 JO o o 300 400 Mannville 450 Manin ilk- 500- Fig 4.19 Plot of Tmax versus Depth for shale samples from wells 6-18-36-6W3 and 3-28-33-23W2 149 Sactsfial co Ssetetiai cc% r«fcff*(ioilj Snlpiiata +_ Reduction $8 Ftfntnlation Ctt| SO, Fig 4.20 Schematic relationship of organic matter diagenesis stages (from Choquette and Pray, 1970) 150 Eogenesis stage, Ro < 0.5-0.7%, hydrocarbon immature. Catagenesis stage, 0.5-0.7% < Ro < 1.3%, oil window. Metagenesis stage, 1.3% < Ro < 2%, gas window In central Saskatchewan, the Ro value for Cretaceous strata is less than 0.4% (Stasiuk et al., 1993), indicating that the Cretaceous strata of this area are in eogenesis stage (Fig.4.21). These rocks are below the thermogenic gas window and gas production is limited to bacterially-generated biogenic methane (Barnes et al, 1990). Fig.4.22 and Fig.4.23 show the relationship of Tmax versus depth, TOC versus depth and HI versus depth of the two sampled wells in central Saskatchewan. In the well 6-18-36-6W3, the TOC and HI values show increasing trends with burial depths, but the Tmax seems relatively scattered. There is a dramatic increase in TOC and HI at the transition from Milk River to Second White Specks. If there was significant generation of gas during the immature stage (eogenesis), both the TOC and hydrogen would be expected to decrease with burial. Actually, they show an increase with burial depth and correlate with Tmax. The increase in HI with thermal maturity means a shift to hydrogen rich organic matter at depth (Price etal., 1999). The TOC and HI increase corresponds to the change of organic matter from predominantly Type III to a greater proportion of Type II. In the well 3-28-33-23W2, the TOC trend dramatically increases at 377m, with organic matter changing from Type III to a mixture of Type II and Type III, but the Tmax and HI are scattered. In summary, the Cretaceous shales in central Saskatchewan have excellent to good potential to generate hydrocarbons, but due to the relatively 151 CD) ° I I I I I I It lOO' E" ?°° Q 300- unnamed Second Sf30C;Ks 400- J* unnamed Viking ^t\J?\Jr~* Mannville OT020406 %. Reflectance in oil Fig 4.21 Ro versus Depth of well 6-18-36-6W3 (From Stasiuk et al, 1993). 152 Depth Vs. TOC of 6-18-36-6W3 Depth Vs Tmxof6-18-36-6W3 Depth Vs. HI of 6-18-36-6W3 TOq%) Tmax(°C) HI 0.0 2.0 4.0 6.0 8.0 10.0 35C 360 370 380 390 400 410 420 430 440 450 0 50 100 150 200 250 300 350 400 100 H • ^~" 200 200- ^^^ ? Lea Park f*50 o s. \ a 300 ! Milk River 300- s s . —*2ndws-r'wfc 350 ~> ~3^ ERpllr..4-nnrrhp " 400 400- 400 - __j»* Weslgale-Fish Scale X \ fc Mannville l-C 500- Fig.4.22 Plots of Rock-Eval Tmax, TOC and HI versus depth of well 6-18-36-6W3 153 Depth Vs. TOC Of 3-28-33-23W2 Depth Vs. Tmx ot 3-28-33-23W2 Depth VS. HI of 3-28-33-23W2 TOC(^ Tmx ("C) HI 390 0 ^00 0 410 0 420 0 130 0 440 0 LOO iv JJJO 4:co a" ooo c o V c WS-lstWS Westgate-Fish Scale fll|P^TW87y~V^il* Fig 4.23 Plots of Rock-Eval Tmax, TOC, HI versus Depth of well 3-28-33-23W2 154 shallow burial, these source rocks have not reached a sufficiently high temperature to produce hydrocarbons. However, this does not mean that there are no possibilities of hydrocarbons migrating from source rocks in other areas to central Saskatchewan, nor does it discount the possibility of finding biogenic gas in central Saskatchewan, as discussed in the next chapter. 4.4 Stable isotopes of carbonate components 4.4.1 Data description Carbon and oxygen isotopes were analyzed from 15 samples taken from the two cores. Four samples were taken from calcite veins, nine were sampled from calcareous sandstones (8 from phase 1 and 1 from phase 2 calcite cement), one was sampled from a calcite strip of glauconitic siltstone and one was sampled from bioclastic mudstone. The results are listed in Table 6, and illustrated in Fig.4.24. According to the petrographic study, most of the samples contain phase 1 calcite cement that precipitated before or during a very early diagenetic stage. The isotope compositions of the Cretaceous calcites in central Saskatchewan are highly variable (Table 6 and Fig 4.24). The 5180 values ranges from -1.75%o to - 16.61%o VPDB, 513C values range from -0.63%o to -23.41 %o VPDB (Table 6). Different carbonate samples fall in different domains in the 513C- 5180 diagram (Fig 4.25). The calcite veins are characterized by higher carbon and oxygen isotope contents. The 5180 and 513C values of phase 1 calcite cements range from -7.73%o to -16.61% VPDB and from -2.04%o to -23.41 %0 VPDB, respectively. 155 Table 6 Results of carbon and oxygen isotope analysis 2004qw82 calcite vein 80 -0.63 -6.75 23.95 127.7 Lea Park Milk 2003QW08 calcite vein 90 -8.72 -13.75 16.74 297.3 River 2003QW23 carbonate 50 -7.00 -9.29 21.33 145.3 2nd WS carbonate 2004qw78 (calcite vein) 90 -1.12 -1.75 29.11 334.3 Lea Park mudstone 2003QW20 (calcite vein) 70 -1.96 -6.43 24.28 479.6 2nd WS mudstone 2004qw51 (Gl&ca strip) 20 -0.80 -9.56 21.06 338.2 Joli Fou Belly 2004qw1 08 sandstone (phi) 50 -6.04 -14.05 16.43 58.5 River Fish 2003QW41 sandstone(phl) 20 -9.16 -13.35 17.15 370 Scale 2004qw42 sandstone(phl) 20 -2.04 -7.73 22.95 495 Cantuar 2003QW87 sandstone(ph1) 40 -23.41 -12.50 18.02 472.5 Cantuar 2004QW31 sandstone(ph1) 40 -6.80 -11.54 19.01 525.6 Cantuar 2004QW37 sandstone(ph1) 45 -8.09 -13.13 17.37 504 Cantuar 2004qw46 sandstone(ph1) 35 -7.47 -8.30 22.35 486.1 Pense 2004qw44 sandstone(phl) 15 -12.84 -16.61 13.79 487.5 Pense 2003QW79 sandstone(ph2) 20 -14.46 -9.59 21.02 450 Cantuar LiPo#3 1.04 -7.94 LiPo#3 0.83 -8.15 LiPo#3 0.93 -8.10 156 18 5'°0(%o,V-PDB; ) -20.00 -15.00 -10.00 -5.00 0.00 I I l I I I I l I l I I I I I L I I I L 0.00 • • A^ -5.00 °1 u \ o -10.00-< • calcite vein "b a A phi calcite cement 00 • Gl&Ca strip -15.00 • bioclasts ph2 calcite cement -20.00 -25.00 Fig 4.24 Carbon versus.Oxygen isotopic composition of calcite cement in central Saskatchewan. 157 5180(%o, V-PDB)/813C (%o, V-PDB) -20.00 -15.00 -10.00 -5.00 0.00 n III U 9% • 50 100 m • »#• - 150 - 200 250 £- Q. # • - 300 g • «* • 350 • • - 400 • # - 450 • V • • 500 • • L 550 • C13 «018 Fig.4.25 Distributions of 513C (%o VPDB) and 5180 (%o VPDB) with respect to depth of calcite cements in central Saskatchewan 158 The 5180 and 513C values of one phase 2 calcite cement from Cantuar sandstone is -9.59%o VPDB and -14.46%o, respectively. One sample of calcite from a fossil in the Second White Specks Formation is characterized by a 5180 of 13 -9.29 %0 and 5 C values of -7.00%o VPDB. The sample of calcite strip from glauconitic siltstone yielded a 5180 value of -9.56%o VPDB and a 513C value of - 0.8%o VPDB. 4.4.2 Interpretation of the results The 5180 values of the calcite cements are controlled by the isotopic composition of the parent fluids and by temperature. If calcite was precipitated from the same fluid and at maximum burial (highest temperature), then we would expect to see a trend of decreasing 5180 with depth. Such a trend is not observed in the samples of this study. (Fig 4.25) The nine samples of phase 1 calcite cement which have an early diagenetic origin can be subdivided into three assemblies. 1) 6 samples from the upper Cantaur Formation and the Pense Formation. 2) 3 samples from the Colorado Group. 3) 1 sample from the Belly River Formation. The Upper Cantuar and Pense Formations formed during the first T-R cycle (Kauffman and Caldwell, 1993), during which the Arctic Ocean water invaded southwards to the latitude of Calgary. The studied area is in the southernmost portion of this transgression and developed in a marginal marine environment. The 5180 and 13 5 C values (-7.73%o to -23.41 %o VPDB and -2.04%o to -23.41 %o VPDB respectively) of the 6 phase 1 calcite cements of assembly 1 are much more 159 depleted than normal seawater at that time, which is about -1%o VPDB (Shackleton and Kennet, 1975). The low 5180 values may indicate involvement of meteoric water in the seawater, in association with the cold water invasion from the Arctic Ocean. The low 513C values may be related to bacterial oxidation of organic carbon. The processes can introduce isotopically light C02 (Longstaffe, 1989) which could enter the porewater, precipitating early diagenetic calcite. The 3 samples of phasel calcite cement (2003qw23, 2003qw41 and 2004qw51) from the Colorado Group have 5180 values ranging from -9.29%o to -13.35%o VPDB, which are significantly lower than the average 5180 value of -1.0%o VPDB of the Cretaceous open oceans (Shackelton and Kennett, 1975, Kyser etal., 1993). The significant depletion of 5180 values indicates either involvement of meteoric water or elevated temperature. Previous studies have shown that in Cretaceous sandstones from the Western Canada Sedimentary Basin, the hydrogen-isotope re-equilibration appears to have occurred at rather low temperatures and the sandstones have experienced an enormous influx of meteoric water (Longstaffe and Ayalon, 1989). Saltzman and Barron (1982) calculated the reasonable temperature range of 5°-16°C for the Late Cretaceous open ocean using the 5180 values of Inoceramid shells from deep sea cores. If we use the calcite-water oxygen isotope fractionation formula of Friedman and O'Neil (1977) to calculate 18 the temperature of calcite precipitation, the 5 0 values from -9.29%0 to -13.35%o VPDB would yield a temperature range of 58.8°C to 90.2°C, which is prohibitively high. A reasonable interpretation of the low 5180 values is that the seawater contains a substantial component of meteoric water. Alternatively, the calcite 160 cements may have formed from meteoric water that infiltrated the sediments in the coastal area during sea-level fall (Taylor etal., 2004). The 513C values range from -0.8%o to -9.1%o VPDB, which are much lower than that of the Cretaceous marine 513C (probably in the range of approximately 0 to +3%o, (Coniglio et al., 2000). The depleted 513C values may have been caused by 1) meteoric water influx that brought in a lower 613C carbon isotope composition from soil-derived C02 (Hutcheon, 1989), or 2) anaerobic microbial oxidation of the organic carbon, introducing carbon isotopically light CO2 (Hutcheon, 1989) because the calcareous sandstones were intimately intercalated with organic-rich shale. The 2 samples from calcite veins filling the synaeresis cracks of the Lea Park Formation yield relatively high 5180 and 513C values of -1.75%o to -6.75%o VPDB and -0.63%o to -1.12%o VPDB respectively. The 613C values seem close to or fall in the range of normal Cretaceous seawater of 0 ~ +3%o (Coniglio et al., 18 2000). Using a Claggett seawater 5 0 value of -1.0%o (Schackelton and Kennett, 1975), the calculated temperatures from these 2 samples range from 17°C to 42.8°C. The temperature of 17°C (for the least 5180-depleted sample) is compatible with the paleotemperature of 15°C -25°C from the isotope composition of the ammonite shells of the Lea Park Formation in central Saskatchewan (Kyser et al., 1993). For the other sample, the low 5180 value is likely caused by the influence of meteoric water. The research of 5180 values from Inoceramids of the Lea Park Formation in Central Saskatchewan done by Kyser, et al. (1993) also concluded that the Claggett seawater was modified by water with lower 5180 values than normal seawater. 161 Chapter 5. Discussion The previous chapters have covered the stratigraphy, sedimentology, and reservoir quality and source rock potential analysis. This chapter will integrate the geological and geochemical analysis to discuss the implications to hydrocarbon exploration and recommendations for future work. 5.1 Sediment sources It is generally agreed that the bulk of sedimentary fill in the Western Canada Sedimentary Basin was derived from the Cordillera to the west, and that minor volumes of sediment may have come from the Canadian Shield to the east (Potocki and Hutcheon, 1992). In southwestern Saskatchewan, the Lower Cantuar Formation changes from fluvial to deltaic facies of flooded valleys northward into marine sandstones, suggesting that the clastic detritus was from the Cordillera (Christopher, 1984). Christopher (1984) further suggested that fluvial quartzose sands of the Mannville Group in the Molanosa area in north- central Saskatchewan and in southeastern Saskatchewan were derived from the Precambrian Shield. Simpson (1975) suggested that the eastern shoreline of the Cretaceous Interior Seaway was located near the northern and eastern edge of the Williston Basin where Lower Cretaceous rocks currently crop out. The westward facies change from more continental to more marine conditions (Fig2.9), as discussed above, is consistent with the proposal that the detritus forming the Mannville succession in the study area was sourced primarily 162 from the east. However, it is worth noting that deposition of the Mannville Group was topographically controlled (Christopher, 2003); thus whether a well has a marine or more fluviatile facies is largely a result of its position relative to Mannville paleotopography. Considering the position of central Saskatchewan in the Western Canada Sedimentary Basin, it is possible that the study area was located on the west-dipping eastern margin of the basin, which later became the interior seaway in post-Mannville time (Williams and Steick, 1975). Sandstones in foredeep settings typically contain moderate to high proportions of recycled sedimentary debris, but little metamorphic and volcanic material and feldspar (Dickinson and Suczek, 1979). The presence of these lithic grains within the Mannville sandstones in the study area is consistent with a source from the Precambrian craton located to the northeast of the study area, although lithic grains are common in Mannville rocks elsewhere. 5.2 Porosity Although depositional processes establish initial porosity and permeability relationships, diagenesis can completely modify or invert these original relationships (Hiatt and Kyser, 2000). Based on observations of thin sections, both primary and secondary porosities are present. Secondary porosity is mainly associated with the dissolution of quartz grains, calcite cements and feldspar. The primary porosity-loss of the Cantuar sandstone is caused by compaction and cementation. For the non-calcareous sandstones, the compaction and quartz overgrowths are the main forces of reducing the primary porosity. For the 163 Calcareous sandstones, the calcite cements play a significant role in destroying the primary porosity. The Phase 1 poikilotopic calcite cement occupies most of the pore spaces resulting in significant porosity reduction in the calcareous sandstone of the Cantuar Formation. The amount of phase 2 calcite cement is small (only found in 1 sample) and is not likely to have played any major role in the porosity-loss of the sandstones. The loss of porosity in the Pense and Viking formations is mainly caused by compaction and cementation. The loss of porosity in the Belly River sandstone is controlled by low texture maturation, calcite cementation and quartz overgrowth. 5.3 Implications for hydrocarbon exploration Saskatchewan has a large amount of crude oil and natural gas resources. The National Energy Board (NEB) estimates the remaining potential crude oil to be 4.2 billion barrels and natural gas to be 4 trillion cubic feet (tcf) (CAPP, 2007). The hydrocarbon is mainly discovered in western, southwest and southeast Saskatchewan. In central Saskatchewan, most of the exploration activities targeted Potash mines since 1950s. Some oil and gas companies such as Shell, Imperial Oil and ConocoPhillips drilled hydrocarbon exploration wells during the1950s to 1960s, but most of the wells turned out to be dry holes and were abandoned. Large amounts of natural gas are thought to exist in shallow, low- permeability Cretaceous sandstones, siltstones, and shales in Saskatchewan. The increased natural gas demands sparked the exploration and development of 164 the unconventional shallow biogenic gas (Shurr and Ridgley, 2002; Pedersen, 2003). Most of the shallow gas pools discovered in Saskatchewan are located in the southwest (Fig 1.1). The shallow gas in southwestern Saskatchewan is mainly hosted in fine-grained siliciclastic reservoirs within the Belle Fourche Formation, the Medicine Hat Member of the Niobrara Formation, and the Milk River Formation (Pedersen, 2003). However, as to central Saskatchewan, based on the regional correlation, the above sandstones thin out and become much shaly and therefore, have decreased reservoir quality. The Rock-Eval analysis indicates that the Colorado source rocks of central Saskatchewan are immature and in eogenesis stage which was an important period when biogenic gas was formed by anaerobic bacteria from organic-rich, thermally immature source rocks at low temperatures (Katz, 1995; Shurr and Ridgley, 2002). The characteristics of shallow biogenic gas can be summarized as: 1) The generation of shallow biogenic gas is initiated shortly after the deposition of source rocks and reservoir (Shurr and Ridgley, 2002); 2) shallow biogenic gas systems are continuous -type accumulations with the source beds and reservoir being very close (Shurr and Ridgley, 2002); 3) low production rate but shallow drilling depth (less than 1000m) make it economic (Yurkowski, 2008). Claypool (1980) suggested that a minimum TOC value of 0.5 % is required for commercial biogenic gas accumulation taking into account both gas saturation and gas losses due to transfer efficiency. The thickness of Cretaceous strata in central Saskatchewan is 515m in well 6-18-36-6W3. The Lower Cretaceous Mannville Group deposited in fluvial to deltaic environment and 165 consists of fluvial- distributary channel sandstones interlaying with flooding plain shale which contains a TOC value of 1.4-2 % with a current depth of less than 600m. This perfect assembly of reservoir and source rock likely make Mannville Group as a shallow gas potential. The Colorado Group is dominated by high organic marine shale with TOC value from 0.27-9.71 % interbedded with minor portion of fine grained sandstone and siltstone. The sandstone and siltstone beds are shaly and very thin and thus, can not form enough storage space for biogenic gas generated from surrounding source rocks. However, the Belly River Formation of the Montana Group consists of thick (59m in the well 6-18-36-6W3) tidal- influenced channel and fluvial channel sands which may possibly provide storage capacity for the Colorado biogenic gas. Although the shallow biogenic gas systems hold important resources to meet increasing energy demands, they are not well defined due to little scientific investigation (Shurr and Ridgley, 2002). For example, the trap mechanism, the critical moment of gas generation, migration and accumulation in a petroleum system are still not well understood (Yurkowski, 2008; Shurr and Ridgley, 2002). 5.4 Recommendation for future studies 1) Structure control The major tectonic zones and elements controlled the sedimentation of the study area. However, the local tectonic adjustment including the activities of the Punnichy Arch that was developed right through the study area (Mossop and Shetsen, 1994) and salt-solution structures associated with the middle Devonian Prairie evaporite (Simpson, 1982) significantly influenced and complicated the 166 stratigraphic architectures (Kauffman and Caldwell, 1993; Mossop and Shetsen, 1994). More detailed investigation is needed to address the activities of the Punnichy Arch during Cretaceous. The time of salt solution and how it related to the deposits and erosion process of Cretaceous strata are not well understood and need further work. The tectonic study will help understand the trap mechanism in the petroleum system in central Saskatchewan. 2) Unconformities Several unconformities exist in Cretaceous strata of central Saskatchewan. Most of the previous studies focused on recognition and descriptions of these unconformities by foraminifera study and stratigraphic correlations. However, the causes for them, especially the unconformities formed during middle to late Cretaceous are not well understood. The relationship between unconformities and the tectonic, the transgression and regression activities in the Western Interior Seaway needs to be further studied. 167 Chapter 6. Conclusions The main purpose of this study was to characterize the lithofacies and identify the depositional environments of each formation of the Cretaceous strata in central Saskatchewan, build a regional stratigraphic framework, understand the diagenetic processes and their influence on reservoir characteristics and quality, and evaluate the hydrocarbon-generative potential of the shales. Based on core logging, stratigraphic correlation, diagenetic and geochemical study, the following conclusions can be made. 1) Facies analysis indicates that the Mannville Group formed in a fluvial-deltaic depositional system, with the Cantuar Formation being mainly formed in fluvial to delta plain environments, and the Pense Formation mainly in marginal marine conditions. The Colorado Group developed under the shelf depositional system and the Montana Group deposited in a coastline-fluvial system. The depositional environments are closely related to sea-level changes. Five late Albian to Campanian regressive pulses represented by the Viking, Belle Fourche, Carlile, Milk River and Belly River formations separated by major marine flooding are recognized. 2) From both southwest and southeast Saskatchewan to central Saskatchewan, the tops of the Mannville and Colorado Groups are getting higher and the overall thickness of Cretaceous strata becomes thinner. Each formation shows distinct gamma-ray and resistivity log patterns and features, but some of them lost their distinguished characteristics in central Saskatchewan due to 168 the stratigraphic complexity and significant thinning. 3) Both primary and secondary porosities are present. Secondary porosity is mainly associated with the dissolution of quartz grains, calcite cements and feldspar. The primary porosity loss of Cantuar sandstone is caused by compaction and cementation. Calcite cements play a significant role in destroying the primary porosity. The Phase 1 poikilotopic calcite cement occupies most of the pore spaces, resulting in significant porosity reduction in the calcareous sandstone of the Cantuar Formation. The porosity loss of the Pense and Viking sandstone is mainly caused by compaction and cementation. 4) The shales within the Cretaceous in central Saskatchewan have excellent to good potential to generate hydrocarbon, but the thermal maturation is low. These rocks are below the thermogenic oil window and gas production is limited to bacterially-generated biogenic methane. 5) Carbon and oxygen isotopes of the calcite cements indicate involvement of meteoric water and oxidation of organic matter in the early stage of diagenesis. 169 References Barnes, M.A., and Bustin, R.M., 1990, Chemistry and diagenesis of organic matter in sediments and fossil fuels. In: Diagenesis (eds. Mcllreath, I.A. and Morrow, D.W.). Geoscience Canada Reprint Series 4, p. 189-204. Beaumont, C, Quinlan, G.M. and Stockmal, G.S., 1993, The evolution of the Western Interior Basin: Causes, consequences and unsolved problems. In: Evolution of the Western Interior Basin (eds. Caldwell, W.G.E. and Kauffman, E. G.). Geological Association of Canada, Special Paper 39, p. 97-117. Blakey, R., 2010, Paleogeography and Geologic Evolution of North America, Images that track the ancient landscapes of North America. NAU Geology, http://jan.ucc.nau.edu/~rcb7/namK75.jpgy Bloch, J., Schroder-Adams, C, Leckie, D.A., Mclntyre, D.J., Craig, J., and Staniland, M., 1993, Revised stratigraphy of the Lower Colorado Group (Albian to Turonian), western Canada. Bulletin of Canadian Petroleum Geology 41, p. 325-348. CAPP (Canadian Association of Petroleum Producers) publication, 2007, Saskatchewan's Oil and Natural Gas Industry Contributing to a Strong Provincial Economy, http://www.capp.ca/getdoc.aspx?DoclD=124350 Choquette, P.W. and Pray, L.C., 1970, Geological nomenclature and classification of porosity in sedimentary carbonates. American Association of Petroleum Geologists, Bulletin 54, p.207-250 Christopher, J.E., 1974, The Upper Jurassic Vanguard and Lower Cretaceous Mannville Groups of southwestern Saskatchewan. Saskatchewan Department of Mineral Resources, Report 151, p. 349. 170 Christopher, J.E., 1984a, Depositional patterns and oilfield trends in the Lower Mesozoic of the northern Williston Basin, Canada; In: Oil and Gas in Saskatchewan (eds. Lorsong, J.A. and Wilson, M.A.). Saskatchewan. Geological Society, Special publication 7, p. 83-102. Christopher, J.E., 1984b, The Lower Cretaceous Mannville Group, northern Williston Basin region, Canada. In: The Mesozoic of Middle North America (eds. Stott, D.F. and Glass, D.G.). Canadian Society of Petroleum Geologists, Memoir 9, p. 109-126. Christopher, J.E., 1999, A note on petroleum occurrences in the Kindersley District, southwestern Saskatchewan. In: Summary of Investigations 1999, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 1999-4.1, p. 33-40. Christopher, J.E., 2000, The Early Mesozoic history of the Punnichy Arch, southeastern Saskatchewan. In: Summary of Investigations 2000, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Misc. Report 2000-4.1, p. 45-58. Christopher, J.E., 2003, Jura-Cretaceous Success Formation and Lower Mannville Group of Saskatchewan. Saskatchewan Industry Resources, Report 223, CD-ROM. Christopher, J.E., and Yurkowski, M., 2003, A major Late Cretaceous (Campanian) unconformity, southeastern Saskatchewan, In: Summary of Investigations 2003, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 2003-4.1, CD- ROM, Paper A-12. Christopher, J.E., and Yurkowski, M., 2004, Geological mapping of Mesozoic strata in southeastern Saskatchewan, northwestern North Dakota, and northeastern Montana, and regional effects of deformation by glacial-ice loading (IEA Weybum C02 Monitoring and Storage Project). In: Summary 171 of Investigations 2004, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 2004-4.1, CD- ROM, Paper A-11, p. 20 Coe, A.L., 2003, Division of the stratigraphical record and geological time. In: The Sedimentary Record of Sea-Level Change (ed. Coe, A.L.). Cambridge University Press, p. 18-33 Coniglio, M., Myrow, P., and White, T., 2000, Stable Carbon and Oxygen Isotope Evidence of CretaceousSea-level Fluctuations Recorded in Septarian Concretations from Pueblo, Colorado, U.S.A. Journal of Sedimentary Research 70, p. 700-714 Craig, H., 1961, Isotopic Variations in Meteoric Water. In: Science 133, p. 1702- 1703 Dickinson, W.R., and Suczek, C.A., 1979, Plate tectonics and sandstone compositions. AAPG Bulletin 63, p. 2164-2182. Dott, R.H., 1964, Wacke, greywacke and matrix—What approach to immature sandstone classification? Journal of Sedimentary Petrology 34, p. 325-632 Eberth, D. A., Dennis R. B., and TokarykT.Y., 1990, Stratigraphy, sedimentology and vertebrate paleontology of the Judith River Formation (Campanian) near Muddy Lake, west-central Saskatchewan. Bulletin of Canadian Petroleum Geology, V. 38, No.4, p.387-406 Espitalie, J., Madec, M., Tissot, B., and Leplat P., 1977, Source Rock Characterization Method for Petroleum Exploration Offshore Technology Conference, paper 2935, Houston, Texas. Folk, R.L., 1974, The petrology of sedimentary rocks. Austin Texas, Hemphill Publishing Co., p. 182 172 Haq, B.U., Hardenbol, J., and Vail, P.R., 1987. Chronology of fluctuating sea levels since the Triassic. Science, v. 235, p. 1156-1166. Hiatt, E.E., and Kyser, K., 2000, Links between depositional and diagenetic processes in basin analysis: porosity and permeability evolution in sediment rocks. In: Fluids and Basin Evolution (ed. Kyser, K.). Mineralogical Association of Canada Short course Series 28, p. 63-92 Issler, D.R., Grist, A.M., and Stasiuk, L.D., 2005, Post-Early Devonian thermal constraints on hydrocarbon source rock maturation in the Keele Tectonic Zone, Tulita area, NWT, Canada, from multi-kinetic apatite fission track thermo chronology, vitrinite reflectance and shale compaction. Bulletin of Canadian Petroleum Geology 53, p. 405-431 Katz, B.J., 1995, Biogenic gas-its formation and economic significance. Proceeding Indonesian Petroleum Association, 24th Annual Convention Kauffman, E.G., 1977, Geological and biological overview: Western Interior Cretaceous basin. Mountain Geologists 14, p. 75-99. Kauffman, E. G., 1977, Geological and biological overview: Western Interior Cretaceous Basin. In: Cretaceous facies, faunas, and paleoenvironments across the Western Interior Basin (ed. Kauffman, E. G.). Mountain Geologist, Rocky Mountain Association of Geologists 14, p. 75 - 99. Kauffman, E. G., 1984, Paleogeography and evolutionary response dynamic in the Cretaceous Western Interior Seaway of North America. In: Jurassic - Cretaceous biochronology and paleogeography of North America (ed. Westerman, G. E. G.). Geological Association of Canada, Special Paper 27, p. 273 - 306. Kauffman, E. G., 1988, The case of the missing community: low-oxygen adapted Paleozoic and Mesozoic bivalves ('flat clams') and bacterial symbioses in 173 typical Phanerozoic areas. In: Abstracts with Programs, Centennial Meeting, Denver, Colorado, Geological Society of America A48. Kauffman, E.G, and Caldwell, W.G.E., 1993, The Western Interior Basin in Space and Time. In: Evolution of the Western Interior Basin (eds. Caldwell, W.G.E., and Kauffman, E.G.). Geological Association of Canada, Special Paper 39, p. 1-30 Kent, D.M. and Christopher J.E., 1994, Geological History of the Williston Basin and Sweetgrass Arch. In: Geological Atlas of the Western Canada Sedimentary Basin (eds. Mossop G.D. and Shetsen I.). Canadian Society of Petroleum Geologists and Alberta Research Council, Special Report 4, p. 421-429. Kyser, T.K., Caldwell, W.G.E., Whittaker, S.G. and Cadrin A.J., 1993, Paleoenvironment and Geochemistry of the northern portion of the Western Interior Seaway during Late Cretaceous time. In: Evolution of the Western Interior Basin (eds. Caldwell, W.G.E., and Kauffman, E.G.). Geological Association of Canada, Special Paper 39, p. 355-378 Lafargue, E., Espitalie, F. M., and Pillot, D., 1998, Rock-Eval 6 Applications in Hydrocarbon Exploration, Production, and Soil Contamination Studies. Oil and Gas Science and Technology 53, p. 421-437 Lafargue, E., Espitilie, J., Marquis, F., and Pillot, D., 2002, Rock-Eval 6 Applications in Hydrocarbon Exploration, Production and in Soil Contamination Studies. Revue de Tlnstut Francais du Petrole 53, p. 421- 437. Leckie, D.A., Bhattacharya, J.P., Bloch J., Gilboy, C.F. and Norris, B., 1994, Cretaceous Colorado/Alberta Group of the Western Canada Sedimentary Basin. In: Geological Atlas of the Western Canada Sedimentary Basin (eds. Mossop G.D. and Shetsen I.). Canadian Society of Petroleum Geologists and Alberta Research Council, Special Report 4, p. 335-352. 174 Leckie, D.A., Kjarsgard, B.A., Bloch, J., Mclntyre, D., Stasiuk, L., and Heaman, L., 1997a, Emplacement and reworking of Cretaceous diamond-bearing crater facies kimberlite of central Saskatchewan, Canada. Geological Society Americian Bulletin 109, p. 1000-1020. Leckie, D.A., Vansbesalaere, N.A., and James, D.P. 1997b, Regional sedimentology, sequence stratigraphy and petroleum geology of the Mannville Group, southwestern Saskatchewan. In: Petroleum Geology of the Cretaceous Mannville Group, Western Canada (eds. Pemberton, S.G., and James, D.P J. Canadian Society of Petroleum Geologists, Memoir 18, p. 211-262. Leckie, D. A., Wallace-Dudley, K.E., Vanbeselaere, N.A., and James, D.P, 2004, Sedimentation in a low-accommodation setting: Nonmarine (Cretaceous) Mannville and marine (Jurassic) Ellis groups, Manyberries field, southeastern Alberta. AAPG Bulletin88, p. 1391-1418 Longstaffe, F.J., and Ayalon, A., 1989, Hydrogen isotope variations of Diagenetic clay minerals from Cretaceous clastic rocks, western Canada sedimentary basin. Ninth International Conference ofAIPEA, Strasbourg, France. Longstaffe, F.J., 1989, Stable isotopes as tracers in clastic diagenesis, In: Short course in Burial Diagenesis (ed. Hutcheon, I.E.). Mineralogical Association of Canada, p.201 -273 Marsh, A., and Heinemann, K., 2005, Report on the regional stratigraphic framework of western Saskatchewan-Phase 1, www.ptrc.ca/.../AA/estern%20Strat%20FrameworkAA/SP%20Final%20Rep Maycock, I.D., 1967, Mannville Group and associated Lower Cretaceous rocks in southwestern Saskatchewan. Saskatchewan Department of Mineral Resources, report96, p. 108. 175 McGookey, D.P., Haun, J.D., Hale, LA., Goodell, H.G., McCubbin, D.G., Weimer, R.J., and Wulf, G.R., 1972, Cretaceous system. In: Geologic Atlas of the Rocky Mountain Region (ed. Mallory, W.), Denver, Colorado. Rocky Mountain Association of Geologists, p. 190-228. McNeil, D.H., and Caldwell, W.G.E., 1981, Cretaceous rocks and their foraminifera in the Manitoba Escarpment. Geological Association of Canada. Special Paper 21, p. 439. Mossop, G.D. and Shetsen, I. (eds.), 1994, Geological atlas of the Western Canada Sedimentary Basin. Canadian Society of Petroleum Geologists and Alberta Research Council, Special Report 4, http://www.ags.gov.ab.ca/publications/wcsb_atlas/atlas.html Nielsen, K.S., Schroder-Adams, C.J., Leckie, DA, 2003, A new stratigraphic framework for the Upper Colorado Group (Cretaceous) in southern Alberta and southwestern Saskatchewan, Canada. Bulletin of Canadian Petroleum Geology 51, p. 304-346. Nielsen, K.S., Schroder-Adams, C. J., Leckie, D.A., Haggart, J.W., and Elberdak, K., 2008, Turonian to Santonian paleoenvironmental changes in the Cretaceous Western Interior Sea: The Carlile and Niobrara Formations in southern Alberta and southwestern Saskatchewan, Canada. Palaeogeography, Palaeoclimatology, Palaeoecology 470, p. 64-91. North, B.R., and Caldwell, W.G.E., 1975, Foraminifera from the Late Cretaceous System of Saskatchewan. In: The Cretaceous System in the Western Interior of North America (ed. Caldwell, W.G.E.). Geological Association of Canada, Special Paper 13, p. 303-331. Pedersen, P.K., 2003, Stratigraphic Relationship of Alderson (Milk River) Strata Between the Hatton and Abbey-Lacadena Pools, Southwestern 176 Saskatchewan-Preliminary Observations. In: Summary of Investigations 2003, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 2003-4.1, CD-ROM, Paper A- 11, P-11- Pedersen, P.K., 2004, Shallow gas research project in southwestern Saskatchewan: Revised lithostratigraphy of the Colorado Group and reservoir architecture of the Belle Fourche and Second White Specks in the Senate Pool. In: Summary of Investigations 2004, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report2004-4.1, CD-ROM, Paper A-16, p.15. Peters, K. E., 1986, Guidelines for evaluating petroleum source rocks using programmed pyrolysis. American Association of Petroleum Geologists Bulletin 70, p. 318-329 Peters, K.E., and Cassa, M.R., 1994, Applied source rock geochemistry. In: The Petroleum System - from source to trap (eds. Magoon, L.B. and Dows, W.G.). AAPG Memoir 60, p.93-117. Pimmel, A., and Claypool, G., 2001, Introduction to shipboard organic geochemistry on the JOIDES Resolution. ODP Tech. Note, 30 [Online]. Available from World Wide Web: Podruski, J.A., Barclay, J.E., Hamblin, A.P., Lee, P.J., Osadetz, K.G., Proctor, R.M., and Taylor, G.C., 1988, Conventional oil reserves of Western Canada (light and medium). In: Geological Atlas of the Western Canada Sedimentary Basin (eds. G.D. Mossop and I. Shetsen). Canadian Society of Petroleum Geologists and Alberta Research Council, Special Report 4, URL Porter, J.W., 1992, Oil and gas reserves of the Western Canada Foreland Basin. In: Foreland Basin and Fold Belt (eds. Macqueen, R.W., and Leckie, D.A.). American Association of Petroleum Geologists, Memoir 55, P. 125-58 177 Potocki, D. and Hutcheon, I.,1992, Lithology and diagenesis of sandstone in the Western Canada Foreland Basin. In: Foreland Basins and Fold Belts (eds. Macqueen, R.W. and Leckie, D.A.). AAPG Memoir 55, p. 229-257. Pratt, L.M., Arthou, M.A., Dean, W.E. and Scholle, P.A., 1993, Paleo- oceanographic cycles and events during the Late Cretaceous in the Western Interior Seaway of North America. In: Evolution of the Western Interior Basin (eds. Caldwell, W.G.E. and Kauffman, E.G.). Geological Association of Canada, Special Paper 39, p. 333-353. Price, L.L., 1963, Lower Cretaceous Rocks of Southeastern Saskatchewan; Geological Survey of Canada, Paper 62-29, p. 55. Price, L.L. and Ball, N.L., 1971, Stratigraphy of the Dual Corporation Potash Shaft No. 1, Saskatoon, Saskatchewan. Geological Survey of Canada, Paper 70-71 Price, L.L. and Ball, N.I., 1973, Stratigraphy of Cominco Potash Shaft NO. 1, Vanscoy, Saskatchewan. Geological Survey of Canada, Paper72-M. Price, LC, Pawlewicz, M., and Daws, T., 1999, Organic Metamorphism in the California petroleum basins, Chapter A-Rock-Eval and vitrinite Reflectance. U.S. Geological Survey Bulletin 2174-A. Ridgley, J.L, McNeil, D.H., Gilboy, C.F., Condon, S.M. and Obradovich, J.D., 2001, Structural and stratigraphic controls on sites of shallow biogenic gas accumulations in the Upper Cretaceous Belle Fourche and Second White Specks-Greenhorn Formations of southern Alberta, Saskatchewan and northern Montana. In: Gas in the Rockies (eds. Anderson, D.S., Robinson, J.W., Estes-Jackson, J.E. and Coalson, E.B.). The Rocky Mountain Association of Geologists, paper 241 -270. 178 Saltzman, E. S., and Barron, E. J., 1982, Deep circulation in the Late Cretaceous: oxygen isotope paleotemperatures from inoceramus remains in DSDP cores. Paleogeography, Palaeoclimatology, Palaeoecology 40, p. 167-181. Saskatchewan Geological Survey (ed. Harper, C.T.), 2003, Geology, and mineral and petroleum resources of Saskatchewan. Saskatchewan Industry and Resources, Miscellaneous Report 2003-7, p. 173. Saskatchewan Ministry of Energy and Resources, 2004, Stratigraphic Correlation Chart, http://www.er.gov.sk.ca/stratchart Shackleton, N.J., and Kennet, J.P., 1975, Late Cenozonic oxygen and carbon isotope change at DSDP site 284: implications for the glacial history of the Northern Hemisphere. In: Initial Reports of the Deep Sea Drilling Project (eds. Kennett, J.P., and Houtz, R.E.) v.29, p.801-807 Schroder-Adams, C.J., Cumbaa, S.L., Bloch, J., Leckie, D.A., Craig, J., Seif El- Dein, S.A., Simons, D.H.A.E., and Kenig, F., 2001, Late Cretaceous (Cenomanian to Campanian) paleoenvironmental history of the Eastern Canadian margin of the Western Interior Seaway: bonebeds and anoxic events. Palaeogeography, Palaeoclimatology, Palaeoecology 170, p. 261- 289. Schroder-Adams, C.J., Leckie, D.A., Bloch, J., Craig, J., Mclntyre, D.J., Adams, P.J., 1996, Paleoenvironmental changes in the Cretaceous (Albian to Turonian) Colorado Group of western Canada: microfossil, sedimentological and geochemical evidence. Cretaceous Research 17, p. 311-365. Shurr, G.W., and Ridgley, J.L., 2002, Unconventional shallow biogenic gas systems. American Association of Petroleum Geololgists Bulletin, v.86, p. 1939-1969. 179 Simpson, F., 1975, Marine lithofacies and biofacies of the Colorado Group (Middle Albian to Santonian) in Saskatchewan. In: The Cretaceous System in the Western Interior of North America (ed. Caldwell, W.G.E.). Geological Association of Canada, Special Paper 13, p. 553-585. Simpson, F., 1982, Sedimentology, Paleoecology and Economic Geology of Lower Colorado (Cretaceous) Sediments, West-central Saskatchewan. Saskatchewan Department of Mineral Resources, Report 150, p. 183. Snowdon L.R., 1989, Organic matter properties and thermal evolution. In: Short course in Burial Diagenesis (ed. Hutcheon, I.E.). Mineralogical Association of Canada, p. 39-58. Stasiuk, L.D., Goodarzi, F. and Potter, J., 1993, Thermal maturity of Mesozoic strata of southern Saskatchewan. Bulletin of Canadian Petroleum Geology, v.41, p. 218-231. Stott, D. F., 1993, Evolution of Cretaceous Foredeeps: A comparative analysis along the length of the Canadian Rocky Mountains. In: Evolution of the Western Interior Basin (eds. Caldwell, W.G.E., and Kauffman, E. G.) Geological Association of Canada, Special Paper 39, p. 131-150. Taylor, K.G., Gaw Thorpe, R.L., and Fannon-Howell, S., 2004, Basin-scale diagenetic alteration of shoreface sandstones in the Upper Cretaceous Spring Canyon and Aberdeen Members, Blackhawk Formation, Book Cliffs, Utah. Sedimentary Geology, v. 172, p. 99-115. Tissot, B.P. and Welte, D.H., 1989, Petroleum Formation and Occurrence Springer-Verlag. Chinese version, published in Beijing Wallace-Dudley, K.E., Leckie, Dale A., Vanbeselaere, N.A and James, D.P, 1998, Regional geology, sedimentology and sequence stratigraphic framework of the Albian Pense Formation, southwestern Saskatchewan. Bulletin of Canada Petroleum Geology, v.46, p. 599-632. 180 Wang, A.Q., Chi, G., and Pedersen, P.K., 2005, Sedimentary and petrographic studies of the Mannville Group in the Saskatoon area, central Saskatchewan: Preliminary results and implications for sediment sources. In: Summary of Investigations 2005, Volume 1. Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 2005- 4.1, CD-ROM, paperA-15, p. 11. Williams, G.D., and Steick, C.R., 1975, Speculation on the Cretaceous Palaeogeography of North America. Geological Association of Canada Special Paper 13, p. 1-19 Yurkowski, M., 2008, Oil & Gas In Saskatchewan Canada. NAPE2008, poster Booth 1027. Yurkowski, M., Marsh, A., and Heinneman, K., 2006, The Niobrara and Carlile Formations of western Saskatchewan - preliminary investigations. In: Summary of Investigations 2006, Volume 1, Saskatchewan Geological Survey, Saskatchewan Industry Resources, Miscellaneous Report 2006- 4.1, CD-ROM, Paper A-14, p.8. 181 Appendix IPL well data retrieved from well tickets 182 Fm Fm Top Fm Top Fm Top Fm Top Thickness UWI Name Subsea (m) TVD(m) Depth (m) (m) 01/01-07-033-04W3/0 CLRD 148.1 173.7 374.9 374.9 01/01-07-033-04W3/0 MNVL -25.6 100.6 548.6 548.6 01/01-07-035-05W3/0 CLRD -30.8 166.7 527 527 01/01-07-035-05W3/0 MNVL -197.5 104 693.7 693.7 01/01-12-030-23W2/0 CLRD 221.9 157.3 293.2 293.2 01/01-12-030-23W2/0 MNVL 64.6 70.1 450.5 450.5 01/01-12-035-26W2/0 CLRD 235 155.4 323.1 323.1 01/01-12-035-26W2/0 MNVL 79.6 106.7 478.5 478.5 01/01-17-027-28W2/0 CLRD 135.9 180.1 476.7 476.7 01/01-17-027-28W2/0 MNVL -44.2 68.6 656.8 656.8 01/01-22-037-01W3/0 CLRD 207.3 142.1 350.5 350.5 01/01-22-037-01W3/0 MNVL 65.2 87.1 492.6 492.6 01/01-24-030-23W2/0 CLRD 226.8 150 286.5 286.5 01/01-24-030-23W2/0 MNVL 76.8 82.3 436.5 436.5 01/01-29-032-01W3/0 CLRD 128 158.2 481.9 481.9 01/01 -29-032-01W3/0 MNVL -30.2 70.1 640.1 640.1 01/01-34-030-23W2/0 CLRD 228.9 153.9 283.5 283.5 01/01-34-030-23W2/0 MNVL 75 58.2 437.4 437.4 01/01-34-037-06W3/0 CLRD 150.6 162.2 362.1 362.1 01/01-34-037-06W3/0 MNVL -11.6 83.2 524.3 524.3 01/01-36-030-23W2/0 CLRD 228.9 155.5 288.3 288.3 01/01-36-030-23W2/0 MNVL 73.4 60 443.8 443.8 01/02-02-034-07W3/0 MNVL -14 109.1 546.8 546.8 01/02-15-032-01W3/0 CLRD 181.6 171 460.9 460.9 01/02-15-032-01W3/0 MNVL 10.6 79.5 631.9 631.9 01/02-25-032-06W3/0 CLRD 122.2 161.5 373.4 373.4 01/02-25-032-06W3/0 MNVL -39.3 68.9 534.9 534.9 01/03-13-038-28W2/0 CLRD 208.9 151 359 359 01/03-13-038-28W2/0 MNVL 57.9 118 510 510 01/03-15-036-09W3/0 CLRD 157.5 146 376 376 01/03-15-036-09W3/0 MNVL 11.5 140 522 522 01/03-20-045-21W2/0 MNVL 210.9 115.5 255.4 255.4 01/03-28-039-04W3/0 CLRD 231.4 158.2 288.6 288.6 01/03-28-039-04W3/0 MNVL 73.2 101.8 446.8 446.8 01/04-02-036-04W3/0 CLRD 122 159.8 402.9 402.9 01/04-02-036-04W3/0 MNVL -37.8 92.6 562.7 562.7 01/04-02-037-06W3/0 CLRD 198.2 159.8 307.8 307.8 01/04-02-037-06W3/0 MNVL 38.4 84.1 467.6 467.6 01/04-02-038-02W3/0 CLRD 210 161.8 359.4 359.4 01/04-02-038-02W3/0 MNVL 48.2 101.5 521.2 521.2 01/04-04-030-20W2/0 CLRD 230.1 153.6 298.4 298.4 01/04-04-030-20W2/0 MNVL 76.5 113.1 452 452 01/04-08-032-09W3/0 CLRD 161.5 184.4 379.2 379.2 01/04-08-032-09W3/0 MNVL -22.9 119.2 563.6 563.6 01/04-10-032-24W2/0 CLRD 238.1 172.6 288.6 288.6 183 01/04-10-032-24W2/0 MNVL 65.5 84.4 461.2 461.2 01/04-10-033-01W3/0 CLRD 168.9 164 368.2 368.2 01/04-10-033-01W3/0 MNVL 4.9 77.4 532.2 532.2 01/04-13-038-28W2/0 CLRD 207.8 150.5 357 357 01/04-13-038-28W2/0 MNVL 57.3 121.5 507.5 507.5 01/04-15-025-08W3/0 CLRD -58.2 195.7 688.2 688.2 01/04-15-025-08W3/0 MNVL -253.9 78.4 883.9 883.9 01/04-16-031-24W2/0 CLRD 140.5 159.4 380.4 380.4 01/04-16-031-24W2/0 MNVL -18.9 69.8 539.8 539.8 01/04-16-037-01W3/0 CLRD 199 141.4 359.7 359.7 01/04-16-037-01W3/0 MNVL 57.6 102.4 501.1 501.1 01/04-20-031-24W2/0 CLRD 136.6 164.6 388 388 01/04-20-031-24W2/0 MNVL -28 68.9 552.6 552.6 01/04-22-031-05 W3/0 CLRD 173.8 176.8 356.6 356.6 01/04-22-031-05 W3/0 MNVL -3 57.3 533.4 533.4 01/04-22-043-02W3/0 CLRD 260.6 164.6 248.1 248.1 01/04-22-043-02W3/0 MNVL 96 126.2 412.7 412.7 01/04-23-041-20W2/0 MNVL 162.8 135.3 393.2 393.2 01/04-26-037-05 W3/0 CLRD 150.2 161.2 353.9 353.9 01/04-26-037-05W3/0 MNVL -11 88.4 515.1 515.1 01/04-29-025-01W3/0 CLRD 126.2 191.7 502.9 502.9 01/04-29-025-01W3/0 MNVL -65.5 67.4 694.6 694.6 01/04-29-026-21W2/0 CLRD 90.2 162.5 444.1 444.1 01/04-29-026-21W2/0 MNVL -72.3 62.4 606.6 606.6 01/04-29-027-22W2/0 CLRD 179.9 167.1 345.3 345.3 01/04-29-027-22W2/0 MNVL 12.8 117.3 512.4 512.4 01/04-29-032-22W2/0 CLRD 254.8 151.8 277.4 277.4 01/04-29-032-22W2/0 MNVL 103 76.8 429.2 429.2 01/04-29-032-28W2/0 CLRD 184.1 169.8 364.5 364.5 01/04-29-032-28W2/0 MNVL 14.3 81.4 534.3 534.3 01/04-29-033-26W2/0 CLRD 198.4 158.5 356 356 01/04-29-033-26W2/0 MNVL 39.9 91.4 514.5 514.5 01/04-29-039-26W2/0 CLRD 239.8 148.4 328.3 328.3 01/04-29-039-26W2/0 MNVL 91.4 96.3 476.7 476.7 01/04-36-039-09W3/0 CLRD 204.2 178.3 290.5 290.5 01/04-36-039-09W3/0 MNVL 25.9 120.7 468.8 468.8 01/05-01-032-06W3/0 CLRD 176.8 204.8 343.8 343.8 01/05-01-032-06W3/0 MNVL -28 66.5 548.6 548.6 01/05-11-025-20W2/0 CLRD 175.9 168.3 383.4 383.4 01/05-11-025-20W2/0 MNVL 7.6 60.9 551.7 551.7 01/05-13-038-28W2/0 CLRD 213.2 155 351 351 01/05-13-038-28W2/0 MNVL 58.2 113 506 506 01/05-14-031-24W2/0 CLRD 237.1 167.6 277.4 277.4 01/05-14-031-24W2/0 MNVL 69.5 66.8 445 445 01/05-15-036-09W3/0 CLRD 137.6 149 398 398 01/05-15-036-09W3/0 MNVL -11.4 120 547 547 01/05-20-032-07W3/0 CLRD 153.9 180.4 381 381 01/05-20-032-07W3/0 MNVL -26.5 142.4 561.4 561.4 184 01/05-21-036-22W2/0 CLRD 242.9 139.3 314.9 314.9 01/05-21-036-22W2/0 MNVL 103.7 131 454.1 454.2 01/05-28-025-28W2/0 CLRD 126.3 208 470 470 01/05-28-025-28W2/0 MNVL -81.7 57 678 678 01/05-31-033-26W2/0 CLRD 180.7 159.4 374.3 374.3 01/05-31-033-26W2/0 MNVL 21.3 88.1 533.7 533.7 01/05-34-030-21W2/0 CLRD 198.4 155.4 341.4 341.4 01/05-34-030-21W2/0 MNVL 43 67.1 496.8 496.8 01/05-34-034-03W3/0 CLRD 137.8 169.2 396.2 396.2 01/05-34-034-03W3/0 MNVL -31.4 118 565.4 565.4 01/06-02-037-21W2/0 CLRD 286.2 159.7 304.8 304.8 01/06-02-037-21W2/0 MNVL 126.5 105.5 464.5 464.5 01/06-10-031-23W2/0 CLRD 243.9 165.8 274.3 274.3 01/06-10-031-23W2/0 MNVL 78.1 87.5 440.1 440.1 01/06-12-038-04W3/0 CLRD 225.8 168.8 283.5 283.5 01/06-12-038-04W3/0 MNVL 57 109.8 452.3 452.3 01/06-13-030-20W2/0 CLRD 241.7 149.3 289.6 289.6 01/06-13-030-20W2/0 MNVL 92.4 67.1 438.9 438.9 01/06-15-036-09W3/0 CLRD 143.3 149 389 389 01/06-15-036-09W3/0 MNVL -5.7 124 538 538 01/06-15-036-25W2/0 CLRD 234.4 152.1 311.5 311.5 01/06-15-036-25W2/0 MNVL 82.3 94.2 463.6 463.6 01/06-16-038-01W3/0 CLRD 220.4 154.3 370 370 01/06-16-038-01W3/0 MNVL 66.1 90.5 524.3 524.3 01/06-19-030-08W3/0 CLRD 126.4 156 412 412 01/06-24-030-28W2/0 CLRD 183.8 155.7 448.1 448.1 01/06-24-030-28W2/0 MNVL 28.1 97.2 603.8 603.8 01/06-25-037-04W3/0 CLRD 202.1 155.5 320 320 01/06-25-037-04W3/0 MNVL 46.6 98.1 475.5 475.5 01/06-27-032-01W3/0 CLRD 257.4 191 330 330 01/06-28-029-24W2/0 CLRD 114.3 155 403.5 403.5 01/06-28-029-24W2/0 MNVL -40.7 46.7 558.5 558.5 01/06-28-031-05W3/0 CLRD 181.1 176 342 342 01/06-36-038-28W2/0 CLRD 225.9 144.5 332.2 332.2 01/06-36-038-28W2/0 MNVL 81.5 102.7 476.6 476.7 01/07-02-038-01W3/0 CLRD 211.8 148.8 375.5 375.5 01/07-02-038-01W3/0 MNVL 63 93.8 524.3 524.3 01/07-11-034-23W2/0 CLRD 241 145.6 301.8 301.8 01/07-14-033-20W2/0 CLRD 238.4 155.8 300.2 300.2 01/07-14-033-20W2/0 MNVL 82.6 7.3 456 456 01/07-20-030-07W3/0 CLRD 162.1 178.6 379.2 379.2 01/07-20-030-07W3/0 MNVL -16.5 59.4 557.8 557.8 01/07-20-034-19W2/0 CLRD 285.3 148.8 256.9 256.9 01/07-20-034-19W2/0 MNVL 136.5 39.3 405.7 405.7 01/07-29-031-22W2/0 CLRD 234.7 131.7 298.7 298.7 01/07-32-039-10W3/0 MNVL 1.2 132.8 517.6 517.6 01/08-12-037-24W2/0 CLRD 254.2 140.2 315.2 315.2 01/08-12-037-24W2/0 MNVL 114 126.8 455.4 455.4 185 01/08-17-032-05W3/0 CLRD 169.5 170.7 356.6 356.6 01/08-17-032-05W3/0 MNVL -1.2 61 527.3 527.3 01/08-29-025-20W2/0 CLRD 170.1 166.7 385.9 385.9 01/08-29-025-20W2/0 MNVL 3.4 53.3 552.6 552.6 01/08-29-031-24W2/0 CLRD 198.7 168.2 321.9 321.9 01/08-29-031-24W2/0 MNVL 30.5 79.9 490.1 490.1 01/08-32-031-21W2/0 CLRD 219.4 142 314.6 314.6 01/08-32-031-21W2/0 MNVL 77.4 58.2 456.6 456.6 01/08-36-031-25W2/0 CLRD 155.8 180.4 374.9 374.9 01/08-36-031-25W2/0 MNVL -24.6 75.6 555.3 555.3 01/09-02-030-20W2/0 CLRD 238.4 152.1 298.4 298.4 01/09-02-030-20W2/0 MNVL 86.3 85.9 450.5 450.5 01/09-02-033-27W2/0 CLRD 215.2 170.1 323.1 323.1 01/09-02-033-27W2/0 MNVL 45.1 92 493.2 493.2 01/09-07-025-02W3/0 CLRD 51.8 171.7 543.3 543.3 01/09-07-025-02W3/0 MNVL -119.9 31.5 715 715 01/09-20-025-21W2/0 CLRD 143.9 164.6 490.7 490.7 01/09-20-025-21W2/0 MNVL -20.7 77.4 655.3 655.3 01/09-29-029-23W2/0 CLRD 226.5 154.9 274.3 274.3 01/09-29-029-23W2/0 MNVL 71.6 93.8 429.2 429.2 01/09-29-030-01W3/0 CLRD 174.1 176.2 477.3 477.3 01/09-29-030-01W3/0 MNVL -2.1 68.9 653.5 653.5 01/09-29-041-05W3/0 CLRD 193.9 155.5 350.5 350.5 01/09-29-041-05W3/0 MNVL 38.4 119.1 506 506 01/09-32-029-10W3/0 CLRD 169.5 199.6 406 406 01/09-32-029-10W3/0 MNVL -30.1 60.1 605.6 605.6 01/10-16-033-20W2/0 CLRD 279.2 153.9 264.6 264.6 01/10-16-033-20W2/0 MNVL 125.3 14.6 418.5 418.5 01/10-20-026-22W2/0 CLRD 66.8 163.7 464.2 464.2 01/10-20-026-22W2/0 MNVL -96.9 79.2 627.9 627.9 01/10-21-032-25W2/0 CLRD 206.3 164.6 334.1 334.1 01/10-21-032-25W2/0 MNVL 41.7 99.3 498.7 498.7 01/10-22-033-27W2/0 CLRD 209.1 174.4 332.2 332.2 01/10-22-033-27W2/0 MNVL 34.7 83.2 506.6 506.6 01/10-29-029-21W2/0 CLRD 212.4 164 323.1 323.1 01/10-29-029-21W2/0 MNVL 48.4 102.4 487.1 487.1 01/11-11-031-11W3/0 CLRD 151.2 191.7 419.7 419.7 01/11-11-031-11W3/0 MNVL -40.5 131.4 611.4 611.4 01/11-12-038-28W2/0 CLRD 217.9 156.1 368.2 368.2 01/11-12-038-28W2/0 MNVL 61.8 87.7 524.3 524.3 01/11-22-025-25W2/0 CLRD 149.5 185 350 350 01/11-22-025-25W2/0 MNVL -35.5 64.5 535 535 01/11-24-038-20W2/0 CLRD 248.1 149.6 341.4 341.4 01/11-24-038-20W2/0 MNVL 98.5 102.1 491 491 01/11-28-037-25W2/0 CLRD 218.2 116.1 359.7 359.7 01/12-02-044-07W3/0 CLRD 122.8 134.1 404.2 404.2 01/12-02-044-07W3/0 MNVL -11.3 163 538.3 538.3 01/12-04-042-19W2/0 CLRD 291.1 136.9 268.2 268.2 186 01/12-04-042-19W2/0 MNVL 154.2 126.2 405.1 405.1 01/12-05-038-03W3/0 CLRD 223.4 165.2 311.5 311.5 01/12-05-038-03W3/0 MNVL 58.2 107.6 476.7 476.7 01/12-10-029-05W3/0 CLRD -8.5 175.9 622.4 622.4 01/12-10-029-05W3/0 MNVL -184.4 40.2 798.3 798.3 01/12-11-038-08W3/0 CLRD 215.8 173.7 286.5 286.5 01/12-11-038-08W3/0 MNVL 42.1 121.1 460.2 460.2 01/12-12-038-28W2/0 MNVL 68.3 125.3 511.5 511.5 01/12-16-026-04W3/0 CLRD -36.6 167 646.2 646.2 01/12-16-026-04W3/0 MNVL -203.6 41.8 813.2 813.2 01/12-16-044-22W2/0 CLRD 297.8 114.3 172.2 172.2 01/12-16-044-22W2/0 MNVL 183.5 235.9 286.5 286.5 01/12-18-033-26W2/0 CLRD 206.7 162.2 349.9 349.9 01/12-18-033-26W2/0 MNVL 44.5 99.6 512.1 512.1 01/12-29-029-19W2/0 CLRD 243.8 152.1 323.1 323.1 01/12-29-029-19W2/0 MNVL 91.7 79.2 475.2 475.2 01/12-30-038-07W3/0 CLRD 210 173.7 301.8 301.8 01/12-30-038-07W3/0 MNVL 36.3 118.9 475.5 475.5 01/13-01-038-08W3/0 CLRD 209.4 175.9 299.6 299.6 01/13-01-038-08W3/0 MNVL 33.5 110.6 475.5 475.5 01/13-03-042-26W2/0 CLRD 259.1 150.6 320 320 01/13-03-042-26W2/0 MNVL 108.5 145.1 470.6 470.6 01/13-04-025-08W3/0 CLRD 63.7 193.8 596.5 596.5 01/13-04-025-08W3/0 MNVL -130.1 72.3 790.3 790.3 01/13-04-027-28W2/0 CLRD 134.4 180.7 486.8 486.8 01/13-04-027-28W2/0 MNVL -46.3 71.3 667.5 667.5 01/13-04-044-09W3/0 CLRD 176.8 178 426.7 426.7 01/13-04-044-09W3/0 MNVL -1.2 145.4 604.7 604.7 01/13-11-037-07W3/0 CLRD 507.8 485.2 0 0 01/13-11-037-07W3/0 MNVL 22.6 95.7 485.2 485.2 01/13-12-038-28W2/0 CLRD 303.5 241.5 268 268 01/13-12-038-28W2/0 MNVL 62 127.8 509.5 509.5 01/13-18-032-05W3/0 CLRD 151.8 177.4 367.3 367.3 01/13-18-032-05W3/0 MNVL -25.6 66.7 544.7 544.7 01/13-21-027-10W3/0 CLRD 0 209.7 643.7 643.7 01/13-21-027-10W3/0 MNVL -209.7 82.3 853.4 853.4 01/13-22-037-08W3/0 CLRD 200.8 169.1 302.1 302.1 01/13-22-037-08W3/0 MNVL 31.7 110.4 471.2 471.2 01/13-23-044-05W3/0 CLRD 157 146.9 330.1 330.1 01/13-23-044-05W3/0 MNVL 10.1 161.6 477 477 01/13-24-031-25W2/0 CLRD 153.6 171 385.3 385.3 01/13-24-031-25W2/0 MNVL -17.4 83.2 556.3 556.3 01/13-30-033-23W2/0 CLRD 239.3 151.2 298.7 298.7 01/13-30-033-23W2/0 MNVL 88.1 74.4 449.9 449.9 01/13-34-033-23W2/0 CLRD 254.8 150.9 291.1 291.1 01/13-34-033-23W2/0 MNVL 103.9 57 442 442 01/14-03-030-20W2/0 CLRD 224.3 143.3 305.1 305.1 01/14-03-030-20W2/0 MNVL 81 89.3 448.4 448.4 187 01/14-06-040-22W2/0 CLRD 208.5 150.3 357.8 357.8 01/14-06-040-22W2/0 MNVL 58.2 94.5 508.1 508.1 01/14-10-027-25W2/0 CLRD 178 201.8 337.7 337.7 01/14-10-027-25W2/0 MNVL -23.8 71.9 539.5 539.5 01/14-10-035-07W3/0 CLRD 166.4 176.7 359.4 359.4 01/14-10-035-07W3/0 MNVL -10.3 99.7 536.1 536.1 01/14-11-028-22W2/0 CLRD 212.7 195.7 310.9 310.9 01/14-11-028-22W2/0 MNVL 17 72.5 506.6 506.6 01/14-20-033-25W2/0 CLRD 214.9 154.8 347.8 347.8 01/14-20-033-25W2/0 MNVL 60.1 74.7 502.6 502.6 01/14-21-031-06W3/0 CLRD 164.6 179.5 356.6 356.6 01/14-21-031-06W3/0 MNVL -14.9 61.3 536.1 536.1 01/14-22-026-26W2/0 CLRD 194.4 192.9 392.9 392.9 01/14-22-026-26W2/0 MNVL 1.5 77.1 585.8 585.8 01/14-28-036-06W3/0 CLRD 189.3 160.9 317.9 317.9 01/14-28-036-06W3/0 MNVL 28.4 93.6 478.8 478.8 01/15-09-026-05W3/0 CLRD -52.2 161.2 664.8 664.8 01/15-09-026-05W3/0 MNVL -213.4 43.3 826 826 01/15-09-037-04W3/0 CLRD 184.7 154.2 329.2 329.2 01/15-09-037-04W3/0 MNVL 30.5 94.8 483.4 483.4 01/15-12-042-22W2/0 CLRD 268.8 171.3 289.6 289.6 01/15-12-042-22W2/0 MNVL 97.5 164.9 460.9 460.9 01/15-14-040-20W2/0 CLRD 280.4 129.8 276.8 276.8 01/15-14-040-20W2/0 MNVL 150.6 132.9 406.6 406.6 01/15-20-033-25W2/0 CLRD 225.8 164.9 335.3 335.3 01/15-20-033-25W2/0 MNVL 60.9 74.7 500.2 500.2 01/15-21-035-19W2/0 CLRD 268.2 162.2 274.3 274.3 01/15-21-035-19W2/0 MNVL 106.1 86.2 436.4 436.5 01/15-24-034-01W3/0 CLRD 178 142.9 349 349 01/15-24-034-01W3/0 MNVL 35.1 99.4 491.9 491.9 01/15-33-031-24W2/0 CLRD 229.6 166.2 281.9 281.9 01/15-33-031-24W2/0 MNVL 63.4 74.9 448.1 448.1 01/16-04-031-23W2/0 CLRD 246.3 164 271.9 271.9 01/16-04-031-23W2/0 MNVL 82.3 87.4 435.9 435.9 01/16-06-031-23W2/0 CLRD 238.6 167.3 271.6 271.6 01/16-06-031-23W2/0 MNVL 71.3 55.5 438.9 438.9 01/16-06-039-07W3/0 CLRD 221.9 185 293.5 293.5 01/16-06-039-07W3/0 MNVL 36.9 115.6 478.5 478.5 01/16-06-039-27W2/0 CLRD 222.8 171.3 335.3 335.3 01/16-06-039-27W2/0 MNVL 51.5 101.2 506.6 506.6 01/16-09-032-08W3/0 CLRD 150.3 170.1 384 384 01/16-09-032-08W3/0 MNVL -19.8 130.2 554.1 554.1 01/16-09-043-21W2/0 MNVL 177.7 167.3 394.4 394.4 01/16-10-040-01W3/0 CLRD 235.6 153.3 308.2 308.2 01/16-10-040-01W3/0 MNVL 82.3 104.8 461.5 461.5 01/16-11-033-01W3/0 CLRD 174.3 167 361.8 361.8 01/16-11-033-01W3/0 MNVL 7.3 75.9 528.8 528.8 01/16-12-031-21W2/0 CLRD 242 148.1 292.6 292.6 188 01/16-12-031-21W2/0 MNVL 93.9 50 440.7 440.7 01/16-16-043-04W3/0 CLRD 235.9 142 289 289 01/16-16-043-04W3/0 MNVL 93.9 164.3 431 431 01/16-18-025-05W3/0 CLRD -9.1 190.2 585.5 585.5 01/16-18-025-05W3/0 MNVL -199.3 80.8 775.7 775.7 01/16-18-030-23W2/0 CLRD 215.7 149.3 289 289 01/16-18-030-23W2/0 MNVL 66.4 74.7 438.3 438.3 01/16-18-039-07W3/0 CLRD 227.9 189.2 289.3 289.3 01/16-18-039-07W3/0 MNVL 38.7 111.3 478.5 478.5 01/16-19-031-08W3/0 MNVL -29.5 111.6 566.9 566.9 01/16-20-037-08W3/0 CLRD 196.3 168.6 304.8 304.8 01/16-20-037-08W3/0 MNVL 27.7 110.6 473.4 473.4 01/16-24-039-04W3/0 CLRD 223.7 154.2 271.3 271.3 01/16-24-039-04W3/0 MNVL 69.5 102.7 425.5 425.5 01/16-25-027-25W2/0 CLRD 201.2 200.6 307.8 307.8 01/16-25-027-25W2/0 MNVL 0.6 82.3 508.4 508.4 01/16-29-033-10W3/0 CLRD 160.6 187.5 394.7 394.7 01/16-29-033-10W3/0 MNVL -26.9 135.9 582.2 582.2 01/16-34-036-25W2/0 CLRD 220.4 121.9 329.2 329.2 01/16-34-036-25W2/0 MNVL 98.6 99.1 451 451.1 01/16-35-040-11W3/0 CLRD 240.9 121 291 291 01/16-36-027-29W2/0 CLRD -67.3 173.5 681.2 681.2 01/16-36-027-29W2/0 MNVL -240.8 71.9 854.7 854.7 01/16-36-036-28W2/0 CLRD 221 153.4 345.9 345.9 01/16-36-036-28W2/0 MNVL 67.6 75.9 499.3 499.3 02/04-02-037-06W3/0 CLRD 194.2 155.8 311.8 311.8 02/04-02-037-06W3/0 MNVL 38.4 85.6 467.6 467.6 02/04-22-043-02W3/0 CLRD 260.6 50.6 248.1 248.1 02/14-06-040-22W2/0 MNVL 58.2 77.1 508.1 508.1 02/16-18-030-23 W2/0 CLRD 216.1 149.3 289 289 02/16-18-030-23 W2/0 MNVL 66.8 74.7 438.3 438.3 03/04-02-037-06W3/0 CLRD 192.7 154.6 313.3 313.3 03/04-02-037-06W3/0 MNVL 38.1 83.2 467.9 467.9 11/01-02-034-20W2/0 CLRD 259.4 160.3 286.5 286.5 11/01-02-034-20W2/0 MNVL 99.1 56.1 446.8 446.8 11/01-02-039-08W3/0 CLRD 223.7 178.6 282.9 282.9 11/01-02-039-08W3/0 MNVL 45.1 119.4 461.5 461.5 11/01-02-044-26W2/0 CLRD 266.8 113 250 250 11/01-02-044-26W2/0 MNVL 153.8 73 363 363 11/01-04-034-20W2/0 CLRD 248.1 152.1 299 299 11/01-04-034-20W2/0 MNVL 96 59.7 451.1 451.1 11/01-04-037-10W3/0 CLRD 88.1 179.5 449 449 11/01-04-037-10W3/0 MNVL -91.4 109.1 628.5 628.5 11/01-10-033-24W2/0 CLRD 233.5 157.9 300.5 300.5 11/01-10-033-24W2/0 MNVL 75.6 73.2 458.4 458.4 11/01-11-037-07W3/0 CLRD 196.3 164.9 310.6 310.6 11/01-11-037-07W3/0 MNVL 31.4 105.8 475.5 475.5 11/01-12-033-24W2/0 CLRD 240.5 153 292.6 292.6 189 11/01-12-033-24W2/0 MNVL 87.5 62.2 445.6 445.6 11/01-12-034-01W3/0 CLRD 152.1 151.8 376.4 376.4 11/01-12-034-01W3/0 MNVL 0.3 93 528.2 528.2 11/01-15-034-25W2/0 CLRD 224.1 146.6 338.3 338.3 11/01-15-034-25W2/0 MNVL 77.5 88.1 484.9 484.9 11/01-15-037-28W2/0 CLRD 225.9 163.4 350.5 350.5 11/01-15-037-28W2/0 MNVL 62.5 98.7 513.9 513.9 11/01-16-036-06W3/0 CLRD 186.6 172.9 319.4 319.4 11/01-16-036-06W3/0 MNVL 13.7 99.3 492.3 492.3 11/01-17-034-01W3/0 CLRD 157 139.3 376.4 376.4 11/01-17-034-01W3/0 MNVL 17.7 77.7 515.7 515.7 11/01-18-030-23W2/0 CLRD 217.3 149.6 289.3 289.3 11/01-18-030-23W2/0 MNVL 67.7 73.8 438.9 438.9 11/01-25-034-01W3/0 CLRD 172.9 148.8 358.1 358.1 11/01-25-034-01W3/0 MNVL 24.1 78.3 506.9 506.9 11/01-25-035-07W3/0 CLRD 179.8 173.1 327.4 327.4 11/01-25-035-07W3/0 MNVL 6.7 107.9 500.5 500.5 11/01-29-033-22 W2/0 CLRD 208.4 157.2 333.8 333.8 11/01-29-033-22 W2/0 MNVL 51.2 55.8 491 491 11/01-31-044-01W3/0 CLRD 280.7 165.5 213.1 213.1 11/01-31-044-01W3/0 MNVL 115.2 153.9 378.6 378.6 11/01-32-036-07W3/0 CLRD 200.9 176.8 304.8 304.8 11/01-32-036-07W3/0 MNVL 24.1 93.3 481.6 481.6 11/01-32-038-07W3/0 CLRD 205.8 167.1 313.9 313.9 11/01-32-038-07W3/0 MNVL 38.7 127.7 481 481 11/01-34-032-25W2/0 CLRD 215.8 148.8 330.7 330.7 11/01-34-032-25W2/0 MNVL 67 92.3 479.5 479.5 11/01-34-035-03W3/0 CLRD 143.5 151.8 378.6 378.6 11/01-34-035-03W3/0 MNVL -8.3 79.2 530.4 530.4 11/01-35-035-25 W2/0 CLRD 223.4 156.6 334.1 334.1 11/01-35-035-25W2/0 MNVL 66.8 88.4 490.7 490.7 11/02-14-038-22W2/0 CLRD 278.8 149.9 295.7 295.7 11/02-14-038-22W2/0 MNVL 128.9 104.3 445.6 445.6 11/03-18-036-03W3/0 CLRD 185 150.8 359.1 359.1 11/03-18-036-03W3/0 MNVL 34.2 105.5 509.9 509.9 11/03-26-032-23W2/0 CLRD 253.1 158 275 275 11/03-26-032-23W2/0 MNVL 95.1 70 433 433 11/03-27-038-27W2/0 CLRD 231.1 160.7 376.7 376.7 11/03-27-038-27W2/0 MNVL 70.4 98.4 537.4 537.4 11/03-30-037-02W3/0 CLRD 199.9 146.9 341.4 341.4 11/03-30-037-02W3/0 MNVL 53 97.2 488.3 488.3 11/04-07-033-22W2/0 CLRD 208.1 149.5 325 325 11/04-07-033-22W2/0 MNVL 58.6 83.5 474.5 474.5 11/04-15-036-03W3/0 MNVL 36.8 92.5 495 495 11/04-16-034-20W2/0 CLRD 250.9 155.2 292.9 292.9 11/04-16-034-20W2/0 MNVL 95.7 60.9 448.1 448.1 11/04-28-029-24W2/0 CLRD 118.8 153.6 397.8 397.8 11/04-28-029-24W2/0 MNVL -34.8 73.7 551.4 551.4 190 11/04-28-033-23W2/0 CLRD 252.7 155.5 287.1 287.1 11/04-28-033-23W2/0 MNVL 97.2 67.3 442.6 442.6 11/04-28-037-07W3/0 CLRD 186.3 155.2 325.2 325.2 11/04-28-037-07W3/0 MNVL 31.1 97.5 480.4 480.4 11/04-36-035-09W3/0 CLRD 146.9 173.1 387.7 387.7 11/04-36-035-09W3/0 MNVL -26.2 123.5 560.8 560.8 11/05-15-036-09W3/0 MNVL -5.8 123.8 541.2 541.2 11/06-04-025-08W3/0 CLRD 52.8 185 570 570 11/06-16-034-27W2/0 CLRD 205.7 158.8 334.4 334.4 11/06-16-034-27W2/0 MNVL 46.9 85.9 493.2 493.2 11/06-29-033-24W2/0 CLRD 189.5 154.5 359.7 359.7 11/06-29-033-24W2/0 MNVL 35 61.3 514.2 514.2 11/07-04-036-03W3/0 MNVL 30.9 110.5 497 497 11/07-22-028-25W2/0 CLRD 57.4 120.7 465.5 465.5 11/08-13-036-07W3/0 CLRD 186.8 167.9 315.5 315.5 11/08-13-036-07W3/0 MNVL 18.9 93.3 483.4 483.4 11/09-06-039-02W3/0 CLRD 219.2 160.9 298.7 298.7 11/09-06-039-02W3/0 MNVL 58.3 85.4 459.6 459.6 11/09-10-036-03W3/0 CLRD 172 137 360.5 360.5 11/09-10-036-03W3/0 MNVL 35 117.2 497.5 497.5 11/09-18-040-07W3/0 CLRD 237.2 173.8 280.4 280.4 11/09-18-040-07W3/0 MNVL 63.4 131 454.2 454.2 11/09-20-034-27W2/0 CLRD 200.3 155.8 343.5 343.5 11/09-20-034-27W2/0 MNVL 44.5 82.6 499.3 499.3 11/09-22-033-23W2/0 CLRD 259.7 151.8 275.8 275.8 11/09-22-033-23W2/0 MNVL 107.9 73.8 427.6 427.6 11/09-26-033-20W2/0 CLRD 248.5 149.1 295 295 11/09-26-033-20W2/0 MNVL 99.4 59.4 444.1 444.1 11/09-26-034-01W3/0 CLRD 184.4 157 344.4 344.4 11/09-26-034-01W3/0 MNVL 27.4 103 501.4 501.4 11/09-27-034-01W3/0 CLRD 189.6 155.8 339.2 339.2 11/09-27-034-01W3/0 MNVL 33.8 98.4 495 495 11/09-28-034-01W3/0 CLRD 188.2 165.5 338.2 338.3 11/09-28-034-01W3/0 MNVL 22.7 84.5 503.7 503.8 11/09-29-033-02W3/0 CLRD 159.7 165.5 379.2 379.2 11/09-29-033-02W3/0 MNVL -5.8 64.9 544.7 544.7 11/09-33-034-01W3/0 CLRD 191.7 155.7 335.9 335.9 11/09-33-034-01W3/0 MNVL 36 104.3 491.6 491.6 11/09-35-034-01W3/0 CLRD 189.3 158.5 337.1 337.1 11/09-35-034-01W3/0 MNVL 30.8 95.7 495.6 495.6 11/10-12-036-07W3/0 CLRD 200.6 182 298 298 11/10-12-036-07W3/0 MNVL 18.6 88.8 480 480 11/11-15-031-27W2/0 CLRD 214.3 172.2 344.4 344.4 11/11-15-031-27W2/0 MNVL 42.1 103.7 516.6 516.6 11/13-07-036-06W3/0 CLRD 213.9 180 285 285 11/13-07-036-06W3/0 MNVL 33.9 109 465 465 11/13-16-030-23W2/0 CLRD 221.9 153.6 290.5 290.5 11/13-16-030-23W2/0 MNVL 68.3 70.1 444.1 444.1 191 11/13-28-038-08W3/0 CLRD 206.4 173.7 292.6 292.6 11/13-28-038-08W3/0 MNVL 32.7 121.7 466.3 466.3 11/13-30-030-19W2/0 CLRD 254.2 154.8 277.1 277.1 11/13-30-030-19W2/0 MNVL 99.4 55.8 431.9 431.9 11/15-17-036-05W3/0 CLRD 176.9 60.5 327.5 327.5 11/15-30-030-23W2/0 CLRD 237.7 158.8 271 271 11/15-30-030-23W2/0 MNVL 78.9 90.8 429.8 429.8 11/16-14-036-23W2/0 CLRD 247.5 159.7 298.7 298.7 11/16-14-036-23W2/0 MNVL 87.8 142.1 458.4 458.4 11/16-16-038-05W3/0 CLRD 220 180.1 295.4 295.4 11/16-16-038-05W3/0 MNVL 39.9 88.4 475.5 475.5 11/16-24-025-02W3/0 CLRD 101.1 158.3 518 518 11/16-25-033-23W2/0 CLRD 169.5 149.7 367 367 11/16-25-033-23W2/0 MNVL 19.8 50 516.7 516.7 12/01-12-033-24W2/0 CLRD 248.1 159.1 285 285 12/01-12-033-24W2/0 MNVL 89 71 444.1 444.1 20/09-06-041-02W3/0 CLRD 243.2 154.2 240.2 240.2 20/09-06-041-02W3/0 MNVL 89 93.9 394.4 394.4 21/01-30-036-25W2/0 CLRD 231.7 140.8 312.7 312.7 21/01-30-036-25W2/0 MNVL 90.9 122 453.5 453.5 21/01-36-038-22W2/0 CLRD 242 153 331 331 21/02-02-044-26W2/0 CLRD 278.9 116.1 239.3 239.3 21/02-02-044-26W2/0 MNVL 162.8 193.8 355.4 355.4 21/02-29-034-28W2/0 CLRD 74.7 154 454 454 21/02-29-034-28W2/0 MNVL -79.3 57 608 608 21/02-30-033-23W2/0 CLRD 228 150.6 310.9 310.9 21/02-30-033-23W2/0 MNVL 77.4 80.4 461.5 461.5 21/03-10-033-01W3/0 CLRD 168.3 158.5 370 370 21/03-10-033-01W3/0 MNVL 9.8 86.2 528.5 528.5 21/03-10-034-23W2/0 CLRD 240.8 153 303.6 303.6 21/03-10-034-23W2/0 MNVL 87.8 52.4 456.6 456.6 21/03-21-035-08W3/0 CLRD 172.2 159.4 334.4 334.4 21/03-21-035-08W3/0 MNVL 12.8 139.3 493.8 493.8 21/04-02-032-25W2/0 CLRD 56.1 163.4 484.6 484.6 21/04-02-032-25W2/0 MNVL -107.3 86 648 648 21/04-04-036-06W3/0 CLRD 176.5 167.9 336.5 336.5 21/04-04-036-06W3/0 MNVL 8.6 104.9 504.4 504.4 21/04-04-037-03W3/0 CLRD 198.2 151.8 345 345 21/04-04-037-03W3/0 MNVL 46.4 88.4 496.8 496.8 21/04-06-035-26W2/0 CLRD 215.2 158.5 323.1 323.1 21/04-06-035-26W2/0 MNVL 56.7 76.2 481.6 481.6 21/04-10-035-08W3/0 CLRD 165.2 182.9 357.5 357.5 21/04-10-035-08W3/0 MNVL -17.7 114 540.4 540.4 21/04-11-035-09W3/0 CLRD 132.9 185.3 404.2 404.2 21/04-11-035-09W3/0 MNVL -52.4 160.3 589.5 589.5 21/04-12-035-09W3/0 CLRD 135.3 176.8 392.9 392.9 21/04-12-035-09W3/0 MNVL -41.5 131.3 569.7 569.7 21/04-13-035-25W2/0 CLRD 200.9 141.8 350.5 350.5 192 21/04-13-035-25W2/0 MNVL 59.1 89 492.3 492.3 21/04-14-034-20W2/0 CLRD 274.6 154.5 272.2 272.2 21/04-14-034-20W2/0 MNVL 120.1 60.4 426.7 426.7 21/04-14-035-22W2/0 CLRD 252.1 135.6 310.9 310.9 21/04-14-035-22W2/0 MNVL 116.5 74.7 446.5 446.5 21/04-14-035-27W2/0 CLRD 190.9 159.5 339.5 339.5 21/04-14-035-27W2/0 MNVL 31.4 84.4 499 499 21/04-16-029-24W2/0 CLRD 125.8 155.1 384.7 384.7 21/04-16-029-24W2/0 MNVL -29.3 70.1 539.8 539.8 21/04-16-035-25W2/0 CLRD 228.3 137.8 326.1 326.1 21/04-16-035-25W2/0 MNVL 90.5 106.1 463.9 463.9 21/04-16-036-07W3/0 CLRD 181.4 168.3 331.6 331.6 21/04-16-036-07W3/0 MNVL 13.1 91.4 499.9 499.9 21/04-16-036-09W3/0 CLRD 165.8 177.6 371.6 371.6 21/04-16-036-09W3/0 MNVL -11.8 115.3 549.2 549.2 21/04-18-026-22W2/0 CLRD -31.1 166.7 557.8 557.8 21/04-18-026-22W2/0 MNVL -197.8 76.2 724.5 724.5 21/04-18-035-08W3/0 CLRD 161.8 181.9 352.7 352.7 21/04-18-035-08W3/0 MNVL -20.1 132.9 534.6 534.6 21/04-18-035-23W2/0 CLRD 218 144.2 344.1 344.1 21/04-18-035-23W2/0 MNVL 73.8 89.3 488.3 488.3 21/04-19-035-26W2/0 CLRD 220.1 159.1 317 317 21/04-19-035-26W2/0 MNVL 61 79.6 476.1 476.1 21/04-19-036-26W2/0 CLRD 212.7 156.3 333.5 333.5 21/04-19-036-26W2/0 MNVL 56.4 78 489.8 489.8 21/04-20-035-08W3/0 CLRD 158.8 175.8 346.6 346.6 21/04-20-035-08W3/0 MNVL -17 124.1 522.4 522.4 21/04-21-036-25W2/0 CLRD 225.5 136.8 335.3 335.3 21/04-21-036-25W2/0 MNVL 88.7 79.6 472.1 472.1 21/04-22-025-23W2/0 CLRD 159.7 171.9 380.7 380.7 21/04-22-025-23W2/0 MNVL -12.2 73.8 552.6 552.6 21/04-22-032-28W2/0 CLRD 191.4 169.7 346.6 346.6 21/04-22-032-28W2/0 MNVL 21.8 90.3 516.2 516.3 21/04-22-035-08W3/0 CLRD 161.6 174.7 344.4 344.4 21/04-22-035-08W3/0 MNVL -13.1 120.4 519.1 519.1 21/04-22-036-02W3/0 CLRD 177.4 152.7 388.3 388.3 21/04-22-036-02W3/0 MNVL 24.7 102.4 541 541 21/04-24-033-24W2/0 CLRD 241.8 155.5 295 295 21/04-24-033-24W2/0 MNVL 86.3 59.7 450.5 450.5 21/04-24-035-08W3/0 CLRD 160.9 175.5 353.6 353.6 21/04-24-035-08W3/0 MNVL -14.6 106.4 529.1 529.1 21/04-24-035-09W3/0 CLRD 164.3 178.3 362.4 362.4 21/04-24-035-09W3/0 MNVL -14 131.7 540.7 540.7 21/04-28-025-26W2/0 CLRD 158.8 192.9 429.5 429.5 21/04-28-025-26W2/0 MNVL -34.1 75 622.4 622.4 21/04-28-030-23W2/0 CLRD 230.4 156.4 279.5 279.5 21/04-28-030-23W2/0 MNVL 74 80.4 435.9 435.9 21/04-28-032-23W2/0 CLRD 251.8 163 276 276 193 21/04-28-032-23W2/0 MNVL 88.8 83 439 439 21/04-28-033-23W2/0 CLRD 243.2 149.9 295.7 295.7 21/04-28-033-23W2/0 MNVL 93.3 75.6 445.6 445.6 21/04-28-035-08W3/0 CLRD 165.5 172.8 338 338 21/04-28-035-08W3/0 MNVL -7.3 114.6 510.8 510.8 21/04-29-034-01W3/0 CLRD 180.4 166.1 347.5 347.5 21/04-29-034-01W3/0 MNVL 14.3 65.5 513.6 513.6 21/04-30-035-08W3/0 CLRD 144.2 183.8 364.8 364.8 21/04-30-035-08W3/0 MNVL -39.6 114 548.6 548.6 21/04-32-034-21W2/0 CLRD 243.3 157.6 307.8 307.8 21/04-32-034-21W2/0 MNVL 85.7 65 465.4 465.4 21/04-34-035-08W3/0 CLRD 168.6 179.3 332.8 332.8 21/04-34-035-08W3/0 MNVL -10.7 106.6 512.1 512.1 21/05-07-036-06W3/0 MNVL 14.3 94.5 482.5 482.5 21/05-10-034-21W2/0 CLRD 260.3 152.1 283.2 283.2 21/05-10-034-21W2/0 MNVL 108.2 67.6 435.3 435.3 21/05-11-037-24W2/0 CLRD 251.7 146.9 322.2 322.2 21/05-11-037-24W2/0 MNVL 104.8 118.6 469.1 469.1 21/05-15-030-23W2/0 CLRD 222.2 150 286.5 286.5 21/05-15-030-23W2/0 MNVL 72.2 78.6 436.5 436.5 21/05-21-032-05W3/0 CLRD 193.4 187 330 330 21/05-30-034-19W2/0 CLRD 290.5 150.9 249.9 249.9 21/05-30-034-19W2/0 MNVL 139.6 50.3 400.8 400.8 21/05-35-031-05W3/0 CLRD 165.2 166.4 360.9 360.9 21/05-35-031-05W3/0 MNVL -1.2 67.4 527.3 527.3 21/06-12-030-11W3/0 CLRD 138.5 172 446 446 21/06-12-030-11W3/0 MNVL -33.5 124 618 618 21/07-30-031-07W3/0 CLRD 136 161.2 402 402 21/08-35-030-28W2/0 CLRD 187.4 155.7 404.2 404.2 21/08-35-030-28W2/0 MNVL 31.7 91.8 559.9 559.9 21/09-27-034-27W2/0 CLRD 210.6 154.9 332.2 332.2 21/09-27-034-27W2/0 MNVL 55.7 85.9 487.1 487.1 21/09-34-033-24W2/0 CLRD 205.7 151.1 333.8 333.8 21/09-34-033-24W2/0 MNVL 54.6 71.4 484.9 484.9 21/10-07-032-05W3/0 CLRD 161.2 184.7 361.8 361.8 21/10-07-032-05W3/0 MNVL -23.5 72.2 546.5 546.5 21/11-12-038-28W2/0 CLRD 217 157.9 368.8 368.8 21/11-12-038-28W2/0 MNVL 59.1 85.6 526.7 526.7 21/12-04-033-23W2/0 CLRD 244.4 157.2 283.5 283.5 21/12-04-033-23W2/0 MNVL 87.2 79 440.7 440.7 21/12-06-027-25W2/0 CLRD 208.2 199.3 335.3 335.3 21/12-06-027-25W2/0 MNVL 8.9 92.1 534.6 534.6 21/12-07-036-02W3/0 CLRD 188.3 159.1 353.6 353.6 21/12-07-036-02W3/0 MNVL 29.2 99.9 512.7 512.7 21/12-11-035-28W2/0 CLRD 177.1 154.6 357.5 357.5 21/12-11-035-28W2/0 MNVL 22.5 123.7 512.1 512.1 21/12-16-033-23W2/0 CLRD 248.4 151.4 283.5 283.5 21/12-16-033-23W2/0 MNVL 97 83.3 434.9 434.9 194 21/12-19-037-04W3/0 CLRD 137.5 148.2 363.9 363.9 21/12-19-037-04W3/0 MNVL -10.7 67.6 512.1 512.1 21/12-20-026-28W2/0 CLRD 136.6 192.7 471.8 471.8 21/12-20-026-28W2/0 MNVL -56.1 61.5 664.5 664.5 21/12-20-030-23W2/0 CLRD 218.3 144.8 287.1 287.1 21/12-20-030-23W2/0 MNVL 73.5 81.1 431.9 431.9 21/12-21-033-25W2/0 CLRD 218.8 157.6 342.9 342.9 21/12-21-033-25W2/0 MNVL 61.2 69.8 500.5 500.5 21/12-22-031-20W2/0 CLRD 167.6 146.3 365.8 365.8 21/12-22-031-20W2/0 MNVL 21.3 96.6 512.1 512.1 21/12-24-034-23W2/0 CLRD 232.2 146.3 317 317 21/12-24-034-23 W2/0 MNVL 85.9 51.8 463.3 463.3 21/12-24-034-27W2/0 CLRD 211.2 162.1 335 335 21/12-24-034-27W2/0 MNVL 49.1 72.9 497.1 497.1 21/12-32-026-28W2/0 CLRD 137.1 192.3 475.2 475.2 21/12-32-026-28W2/0 MNVL -55.2 68 667.5 667.5 21/12-32-033-25W2/0 CLRD 225.8 156 341.4 341.4 21/12-32-033-25W2/0 MNVL 69.8 81.7 497.4 497.4 21/12-32-034-02W3/0 CLRD 163.9 149.6 372.2 372.2 21/12-32-034-02W3/0 MNVL 14.3 78.7 521.8 521.8 21/12-34-033-21W2/0 CLRD 247.2 150.2 289.6 289.6 21/12-34-033-21W2/0 MNVL 97 66.2 439.8 439.8 21/13-01-037-08W3/0 CLRD 199.4 169.2 307.8 307.8 21/13-01-037-08W3/0 MNVL 30.2 111.3 477 477 21/13-11-034-01W3/0 CLRD 174.6 157.9 354.2 354.2 21/13-11-034-01W3/0 MNVL 16.7 79.2 512.1 512.1 21/13-11-034-03W3/0 CLRD 175.3 173.8 356.6 356.6 21/13-11-034-03W3/0 MNVL 1.5 89.3 530.4 530.4 21/13-14-036-03W3/0 CLRD 176.6 138 347 347 21/13-14-036-03W3/0 MNVL 38.6 102 485 485 21/13-16-035-21W2/0 CLRD 271 149.4 292.6 292.6 21/13-16-035-21W2/0 MNVL 121.6 60.3 442 442 21/14-12-038-28W2/0 CLRD 285.1 231.5 290.5 290.5 21/14-12-038-28W2/0 MNVL 53.6 85.3 522 522 21/15-21-036-08W3/0 CLRD 187.7 172.8 314.9 314.9 21/15-21-036-08W3/0 MNVL 14.9 104.8 487.7 487.7 21/16-18-030-23W2/0 CLRD 215.4 152.7 289 289 21/16-18-030-23W2/0 MNVL 62.7 74 441.7 441.7 21/16-20-032-04W3/0 CLRD 169.8 173.1 381 381 21/16-20-032-04W3/0 MNVL -3.3 81.1 554.1 554.1 22/04-20-035-08W3/0 CLRD 143.7 161.3 361.7 361.7 22/04-20-035-08W3/0 MNVL -17.6 106 523 523 22/04-29-034-01W3/0 CLRD 177.1 154 351.4 351.4 22/04-29-034-01W3/0 MNVL 23.1 97.5 505.4 505.4 30/06-29-030-21W2/0 CLRD 215.8 161.8 323.1 323.1 30/06-29-030-21W2/0 MNVL 54 67.7 484.9 484.9 31/01-04-029-22W2/0 CLRD 227.6 158.8 289.6 289.6 31/01-04-029-22W2/0 MNVL 68.8 82.3 448.4 448.4 195 31/01 -15-026-02 W3/0 CLRD 90.4 165.4 514.6 514.6 31/01-15-026-02W3/0 MNVL -75 69 680 680 31/01-20-033-23W2/0 MNVL 93.8 76.2 442 442 31/02-20-042-05 W3/0 CLRD 219.7 149 322.5 322.5 31/02-20-042-05W3/0 MNVL 70.7 141.1 471.5 471.5 31/02-21-034-27W2/0 CLRD 195.4 144.5 350.5 350.5 31/02-21-034-27W2/0 MNVL 50.9 76.2 495 495 31/03-21-031-19W2/0 CLRD 234.7 151.2 292 292 31/03-21-031-19W2/0 MNVL 83.5 60 443.2 443.2 31/04-10-025-23W2/0 CLRD 161.9 173.7 374.9 374.9 31/04-10-025-23W2/0 MNVL -11.8 67.1 548.6 548.6 31/04-10-033-01W3/0 CLRD 170.4 167 366 366 31/04-10-033-01W3/0 MNVL 3.4 74 533 533 31/04-10-034-27W2/0 CLRD 203.6 152.4 341.4 341.4 31/04-10-034-27W2/0 MNVL 51.2 85.3 493.8 493.8 31/04-15-036-09W3/0 CLRD 152.6 158 382 382 31/04-15-036-09W3/0 MNVL -5.4 127 540 540 31/05-04-035-27W2/0 CLRD 186.2 153.9 362.7 362.7 31/05-04-035-27W2/0 MNVL 32.3 77.8 516.6 516.6 31/05-13-038-28W2/0 CLRD 224.7 165.8 338.3 338.3 31/05-13-038-28W2/0 MNVL 58.9 90.9 504.1 504.1 31/05-18-034-25W2/0 CLRD 148.1 160 417.9 417.9 31/05-18-034-25W2/0 MNVL -11.9 98.8 577.9 577.9 31/05-26-035-01W3/0 CLRD 197.8 150.6 344.4 344.4 31/05-26-035-01W3/0 MNVL 47.2 109.7 495 495 31/05-29-034-27W2/0 CLRD 203.6 154.2 346.9 346.9 31/05-29-034-27W2/0 MNVL 49.4 91.4 501.1 501.1 31/05-30-036-06W3/0 CLRD 193 164.6 313.9 313.9 31/05-30-036-06W3/0 MNVL 28.4 97.6 478.5 478.5 31/05-30-041-27W2/0 CLRD 149.3 159.4 378 378 31/05-30-041-27W2/0 MNVL -10.1 117 537.4 537.4 31/05-31-029-20W2/0 CLRD 214.3 154.3 320 320 31/05-31-029-20W2/0 MNVL 60 96.3 474.3 474.3 31/05-33-034-27W2/0 CLRD 209.1 157.3 336.2 336.2 31/05-33-034-27W2/0 MNVL 51.8 91.7 493.5 493.5 31/05-33-043-22W2/0 CLRD 295.3 132.2 245.4 245.4 31/05-33-043-22W2/0 MNVL 163.1 171 377.6 377.6 31/05-34-035-02W3/0 CLRD 178 153.3 349.6 349.6 31/05-34-035-02W3/0 MNVL 24.7 99.7 502.9 502.9 31/06-16-036-03W3/0 CLRD 187.5 150.9 342.9 342.9 31/06-16-036-03W3/0 MNVL 36.6 115.8 493.8 493.8 31/07-22-039-07W3/0 CLRD 228 180.7 297.8 297.8 31/07-22-039-07W3/0 MNVL 47.3 154.9 478.5 478.5 31/08-25-030-24W2/0 CLRD 226.8 149.1 280.4 280.4 31/08-25-030-24W2/0 MNVL 77.7 82.6 429.5 429.5 31/09-04-032-05W3/0 CLRD 149.7 178.4 377.3 377.3 31/09-04-032-05W3/0 MNVL -28.6 59.1 555.6 555.7 31/11-02-031-07W3/0 CLRD 160.2 180.5 375 375 196 31/11-09-036-03W3/0 CLRD 184.4 150.5 353.6 353.6 31/11-09-036-03W3/0 MNVL 33.9 72 504.1 504.1 31/11-11-033-01W3/0 CLRD 167.3 156.5 370 370 31/11-11-033-01W3/0 MNVL 10.8 75.5 526.5 526.5 31/11-12-038-28W2/0 CLRD 217.1 157.9 364.5 364.5 31/11-12-038-28W2/0 MNVL 59.2 82.6 522.4 522.4 31/12-04-033-23W2/0 CLRD 244.4 157.3 284.4 284.4 31/12-04-033-23W2/0 MNVL 87.1 78.9 441.7 441.7 31/12-10-038-28W2/0 CLRD 219.2 170.1 343.5 343.5 31/12-10-038-28W2/0 MNVL 49.1 80.8 513.6 513.6 31/12-16-036-03W3/0 CLRD 197.3 163.7 329 329 31/12-16-036-03W3/0 MNVL 33.6 82.3 492.7 492.7 31/12-19-036-23W2/0 CLRD 254.5 153.3 323.1 323.1 31/12-19-036-23W2/0 MNVL 101.3 132.9 476.3 476.4 31/12-20-032-05W3/0 CLRD 164.6 178.6 356.9 356.9 31/12-20-032-05W3/0 MNVL -14 64.7 535.5 535.5 31/12-22-030-25W2/0 CLRD 125.9 148.2 421.5 421.5 31/12-22-030-25W2/0 MNVL -22.3 76.5 569.7 569.7 31/13-01-035-08W3/0 CLRD 164.3 173.1 362.7 362.7 31/13-01-035-08W3/0 MNVL -8.8 125.6 535.8 535.8 31/13-02-036-03W3/0 CLRD 176.1 149.6 353 353 31/13-02-036-03W3/0 MNVL 26.5 98.5 502.6 502.6 31/13-04-033-21W2/0 CLRD 237.5 157.9 301.1 301.1 31/13-04-033-21W2/0 MNVL 79.6 100.6 459 459 31/13-04-035-21W2/0 CLRD 258.8 151.2 298.7 298.7 31/13-04-035-21W2/0 MNVL 107.6 62.8 449.9 449.9 31/13-06-034-19W2/0 CLRD 281.1 154.6 263 263 31/13-06-034-19W2/0 MNVL 126.5 67.6 417.6 417.6 31/13-06-035-19W2/0 CLRD 287.1 146.3 262.1 262.1 31/13-06-035-19W2/0 MNVL 140.8 53.7 408.4 408.4 31/13-06-035-21W2/0 CLRD 254.2 147.5 309.7 309.7 31/13-06-035-21W2/0 MNVL 106.7 77.7 457.2 457.2 31/13-11-033-23W2/0 CLRD 260.3 162.4 271 271 31/13-11-033-23W2/0 MNVL 97.9 70.7 433.4 433.4 31/13-11-035-08W3/0 CLRD 168.5 174.6 353.6 353.6 31/13-11-035-08W3/0 MNVL -6.1 111.9 528.2 528.2 31/13-12-040-08W3/0 CLRD 221.9 176.7 295.7 295.7 31/13-12-040-08W3/0 MNVL 45.2 125 472.4 472.4 31/13-14-037-09W3/0 CLRD 203 183.1 302.4 302.4 31/13-14-037-09W3/0 MNVL 19.9 114.3 485.5 485.5 31/13-15-031-06W3/0 CLRD 179 201 345 345 31/13-15-031-06W3/0 MNVL -22 66 546 546 31/13-16-035-08W3/0 CLRD 161.9 174.4 345 345 31/13-16-035-08W3/0 MNVL -12.5 105.4 519.4 519.4 31/13-16-035-27W2/0 CLRD 193.6 159.4 362.7 362.7 31/13-16-035-27W2/0 MNVL 34.2 75.3 522.1 522.1 31/13-18-025-27W2/0 CLRD 155.2 206.7 432.8 432.8 31/13-18-025-27W2/0 MNVL -51.5 64.6 639.5 639.5 197 31/13-18-030-20W2/0 CLRD 206.9 154.2 323.1 323.1 31/13-18-030-20W2/0 MNVL 52.7 71.3 477.3 477.3 31/13-18-033-22W2/0 CLRD 207.6 147.8 329.2 329.2 31/13-18-033-22W2/0 MNVL 59.8 65.5 477 477 31/13-19-033-25W2/0 CLRD 221.9 161 344.4 344.4 31/13-19-033-25W2/0 MNVL 60.9 87.1 505.4 505.4 31/13-21-029-20W2/0 CLRD 217.3 159.7 312.4 312.4 31/13-21-029-20W2/0 MNVL 57.6 82.6 472.1 472.1 31/13-22-025-25W2/0 MNVL -36.3 65.2 538.9 538.9 31/13-22-037-04W3/0 CLRD 188.7 152.4 320 320 31/13-22-037-04W3/0 MNVL 36.3 104.9 472.4 472.4 31/13-23-035-08W3/0 CLRD 160 170.4 347.2 347.2 31/13-23-035-08W3/0 MNVL -10.4 110.9 517.6 517.6 31/13-23-037-05W3/0 CLRD 140.2 161.9 362.7 362.7 31/13-23-037-05W3/0 MNVL -21.7 85 524.6 524.6 31/13-24-029-21W2/0 CLRD 189.5 155.7 346.6 346.6 31/13-24-029-21W2/0 MNVL 33.8 103.6 502.3 502.3 31/13-24-036-03W3/0 CLRD 179.8 149.3 354.2 354.2 31/13-24-036-03W3/0 MNVL 30.5 98.2 503.5 503.5 31/13-25-032-24W2/0 CLRD 227.5 142 303 303 31/13-25-032-24W2/0 MNVL 85.5 64 445 445 31/13-29-033-21W2/0 CLRD 239.6 159.1 298.7 298.7 31/13-29-033-21W2/0 MNVL 80.5 51.8 457.8 457.8 31/13-30-033-23W2/0 CLRD 239.6 151.2 298.7 298.7 31/13-30-033-23W2/0 MNVL 88.4 74.4 449.9 449.9 31/14-08-032-04W3/0 CLRD 142.7 176.8 384 384 31/14-08-032-04W3/0 MNVL -34.1 73.2 560.8 560.8 31/14-15-025-23W2/0 CLRD 153.2 168 387 387 31/14-15-025-23W2/0 MNVL -14.8 62 555 555 31/14-22-033-21W2/0 CLRD 251.1 151.8 289.6 289.6 31/14-22-033-21W2/0 MNVL 99.3 81.6 441.4 441.4 31/14-29-035-08W3/0 CLRD 166.7 185.3 342.6 342.6 31/14-29-035-08W3/0 MNVL -18.6 115.8 527.9 527.9 31/15-11-032-27W2/0 CLRD 197.5 154.9 338.3 338.3 31/15-11-032-27W2/0 MNVL 42.6 70.4 493.2 493.2 31/15-17-030-20W2/0 CLRD 202.1 153.6 329.2 329.2 31/15-17-030-20W2/0 MNVL 48.5 93.3 482.8 482.8 31/15-17-036-05W3/0 CLRD 186.5 172.2 315.5 315.5 31/15-17-036-05W3/0 MNVL 14.3 103 487.7 487.7 31/15-22-026-26W2/0 CLRD 196 191.1 388 388 31/15-22-026-26W2/0 MNVL 4.9 78.4 579.1 579.1 31/15-34-032-28W2/0 CLRD 197.2 175.2 340.5 340.5 31/15-34-032-28W2/0 MNVL 22 93.3 515.7 515.7 31/15-34-037-27W2/0 CLRD 224.9 173.7 354.8 354.8 31/15-34-037-27W2/0 MNVL 51.2 100 528.5 528.5 31/15-36-032-29W2/0 CLRD 184.4 162.1 352.7 352.7 31/15-36-032-29W2/0 MNVL 22.3 82.6 514.8 514.8 31/16-02-030-21W2/0 CLRD 212.2 159.8 313.9 313.9 198 31/16-02-030-21W2/0 MNVL 52.5 93.8 473.6 473.7 31/16-06-035-08W3/0 CLRD 158.5 177.7 349.6 349.6 31/16-06-035-08W3/0 MNVL -19.2 114.3 527.3 527.3 31/16-10-044-27W2/0 CLRD 216.4 142.6 310.9 310.9 31/16-10-044-27W2/0 MNVL 73.8 162.2 453.5 453.5 31/16-12-034-24W2/0 CLRD 230.7 142.7 311.5 311.5 31/16-12-034-24W2/0 MNVL 88 75.5 454.2 454.2 31/16-15-034-27W2/0 CLRD 210.6 151.2 335.3 335.3 31/16-15-034-27W2/0 MNVL 59.4 88.4 486.5 486.5 31/16-26-036-07W3/0 MNVL 24.8 96 481 481 41/01-04-037-28W2/0 CLRD 229.2 162.5 357.2 357.2 41/01-04-037-28W2/0 MNVL 66.7 101.2 519.7 519.7 41/01-12-034-01W3/0 CLRD 151.2 151.8 376.4 376.4 41/01-12-034-01W3/0 MNVL -0.6 93 528.2 528.2 41/01-13-032-20W2/0 CLRD 212.1 146.9 317 317 41/01-13-032-20W2/0 MNVL 65.2 109.1 463.9 463.9 41/01-22-036-03W3/0 CLRD 176 141.5 344 344 41/01-22-036-03W3/0 MNVL 34.5 103.5 485.5 485.5 41/01-22-039-08W3/0 CLRD 229.2 182.9 240.8 240.8 41/01-22-039-08W3/0 MNVL 46.3 140.5 423.7 423.7 41/01-28-034-20W2/0 CLRD 283.5 156.4 262.4 262.4 41/01-28-034-20W2/0 MNVL 127.1 59.7 418.8 418.8 41/01-29-043-10W3/0 MNVL 36.5 152.7 562.7 562.7 41/03-29-025-22W2/0 CLRD 20.5 154.2 512.8 512.8 41/04-29-025-01W3/0 CLRD 131.9 223.6 499.2 499.2 41/04-29-033-02W3/0 CLRD 149.7 157.5 390 390 41/04-29-033-02W3/0 MNVL -7.8 73.5 547.5 547.5 41/05-22-034-01W3/0 MNVL 18.3 92.7 509.3 509.3 41/06-10-031-23W2/0 CLRD 239.6 159.7 278.6 278.6 41/06-10-031-23W2/0 MNVL 79.9 86.6 438.3 438.3 41/06-15-031-04W3/0 CLRD 157.8 168 418 418 41/07-11-035-21W2/0 CLRD 269.1 143.8 284.4 284.4 41/07-11-035-21W2/0 MNVL 125.3 80.8 428.2 428.2 41/08-02-033-23W2/0 CLRD 252.1 148.1 278.6 278.6 41/08-02-033-23W2/0 MNVL 104 94.5 426.7 426.7 41/08-03-033-23W2/0 CLRD 256.1 151.5 274.3 274.3 41/08-03-033-23W2/0 MNVL 104.6 87.8 425.8 425.8 41/08-07-030-20W2/0 CLRD 216.1 153.3 317.6 317.6 41/08-07-030-20W2/0 MNVL 62.8 102.7 470.9 470.9 41/08-11-037-06W3/0 CLRD 93.8 156 410.6 410.6 41/08-11-037-06W3/0 MNVL -62.2 79.6 566.6 566.6 41/08-12-034-27W2/0 CLRD 183.5 150 362.7 362.7 41/08-12-034-27W2/0 MNVL 33.5 84.7 512.7 512.7 41/08-20-033-20W2/0 CLRD 263.7 150.9 286.5 286.5 41/08-20-033-20W2/0 MNVL 112.8 64.6 437.4 437.4 41/08-22-033-20W2/0 CLRD 246.6 153.3 297.2 297.2 41/08-22-033-20W2/0 MNVL 93.3 58.5 450.5 450.5 41/08-22-036-07W3/0 CLRD 186 166.8 326.4 326.4 199 41/08-22-036-07W3/0 MNVL 19.2 99.9 493.2 493.2 41/08-24-030-24W2/0 CLRD 211.2 147.2 295.7 295.7 41/08-24-030-24W2/0 MNVL 64 83.5 442.9 442.9 41/08-28-027-26W2/0 CLRD 181.7 192.9 444.7 444.7 41/08-28-027-26W2/0 MNVL -11.2 87.2 637.6 637.6 41/08-34-034-01W3/0 CLRD 188.6 154.8 334.7 334.7 41/08-34-034-01W3/0 MNVL 33.8 92.1 489.5 489.5 41/08-36-033-21W2/0 CLRD 264.5 151.5 277.4 277.4 41/08-36-033-21W2/0 MNVL 113 76.2 428.9 428.9 41/09-26-033-23W2/0 CLRD 243.6 155.5 293.8 293.8 41/09-26-033-23W2/0 MNVL 88.1 51.5 449.3 449.3 41/09-29-036-01W3/0 CLRD 202.7 156.3 359.7 359.7 41/09-29-036-01W3/0 MNVL 46.4 72.3 516 516 41/10-29-036-09W3/0 CLRD 176.6 184.1 350.4 350.5 41/10-29-036-09W3/0 MNVL -7.5 125.9 534.5 534.6 41/11-12-038-28W2/0 CLRD 215.8 157.2 359.4 359.4 41/11-12-038-28W2/0 MNVL 58.6 102.8 516.6 516.6 41/13-10-027-02W3/0 CLRD 24.7 175.2 589.8 589.8 41/13-10-027-02W3/0 MNVL -150.5 67.1 765 765 41/13-11-031-25W2/0 CLRD 161.3 164.9 390.1 390.1 41/13-11 -031-25W2/0 MNVL -3.6 72.9 555 555 41/13-22-034-01W3/0 CLRD 170.7 147.8 353.6 353.6 41/13-22-034-01W3/0 MNVL 22.9 80.8 501.4 501.4 41/13-24-035-25W2/0 CLRD 218.2 149.9 341.4 341.4 41/13-24-035-25W2/0 MNVL 68.3 123.2 491.3 491.3 41/13-33-032-28W2/0 CLRD 184.4 175 351.7 351.7 41/13-33-032-28W2/0 MNVL 9.4 70.4 526.7 526.7 41/13-33-037-01W3/0 CLRD 199 143.3 374.9 374.9 41/13-33-037-01W3/0 MNVL 55.7 78.3 518.2 518.2 41/13-36-041-04W3/0 CLRD 220.7 158.5 304.8 304.8 41/13-36-041-04W3/0 MNVL 62.2 117 463.3 463.3 41/14-14-030-21W2/0 CLRD 211.3 163.4 325.1 325.2 41/14-14-030-21W2/0 MNVL 48.1 74.1 488.3 488.6 41/14-23-034-03W3/0 CLRD 186.3 168.3 350.5 350.5 41/14-23-034-03W3/0 MNVL 18 111.5 518.8 518.8 41/15-02-037-06W3/0 CLRD 171.3 158.8 333.8 333.8 41/15-02-037-06W3/0 MNVL 12.5 80.1 492.6 492.6 41/15-16-029-24W2/0 CLRD 60 155.5 451.1 451.1 41/15-16-029-24W2/0 MNVL -95.5 110.9 606.6 606.6 41/15-17-035-08W3/0 CLRD 145.2 161 362 362 41/15-17-035-08W3/0 MNVL -15.8 122.6 523 523 41/15-32-031-27W2/0 CLRD 196.3 168.5 353.6 353.6 41/15-32-031-27W2/0 MNVL 27.8 94.2 522.1 522.1 41/15-32-034-08W3/0 MNVL -39.3 122.8 557.8 557.8 41/15-36-032-27W2/0 CLRD 204.9 164.6 326.1 326.1 41/15-36-032-27W2/0 MNVL 40.3 91.5 490.7 490.7 41/16-06-035-08W3/0 CLRD 158.5 177.7 349.6 349.6 41/16-06-035-08W3/0 MNVL -19.2 114.3 527.3 527.3 200 41/16-06-037-08W3/0 CLRD 188.1 169.5 311.8 311.8 41/16-06-037-08W3/0 MNVL 18.6 112.1 481.3 481.3 41/16-08-027-01W3/0 CLRD 138.4 176.8 487.7 487.7 41/16-08-027-01W3/0 MNVL -38.4 40.8 664.5 664.5 41/16-08-035-08W3/0 CLRD 160.3 175.9 350.5 350.5 41/16-08-035-08W3/0 MNVL -15.6 124.3 526.4 526.4 41/16-09-035-01W3/0 CLRD 199.3 150.3 329.2 329.2 41/16-09-035-01W3/0 MNVL 49 98.1 479.5 479.5 41/16-10-030-22W2/0 CLRD 229.5 160 301.8 301.8 41/16-10-030-22W2/0 MNVL 69.5 62.5 461.8 461.8 41/16-11-032-22W2/0 CLRD 257.9 158.2 279.5 279.5 41/16-11-032-22W2/0 MNVL 99.7 68.9 437.7 437.7 41/16-11-034-02W3/0 CLRD 159.4 153 381 381 41/16-11-034-02W3/0 MNVL 6.4 73.2 534 534 41/16-12-034-20W2/0 CLRD 278.9 152.4 265.2 265.2 41/16-12-034-20W2/0 MNVL 126.5 51.8 417.6 417.6 41/16-12-034-21W2/0 CLRD 270 152.7 272.2 272.2 41/16-12-034-21W2/0 MNVL 117.3 61.6 424.9 424.9 41/16-14-034-01W3/0 CLRD 179.9 151.5 344.4 344.4 41/16-14-034-01W3/0 MNVL 28.4 91.8 495.9 495.9 41/16-16-039-08W3/0 CLRD 220.3 182.9 278 278 41/16-16-039-08W3/0 MNVL 37.4 126.4 460.9 460.9 41/16-17-037-03W3/0 CLRD 210.3 163.7 382.8 382.8 41/16-17-037-03W3/0 MNVL 46.6 82.3 546.5 546.5 41/16-18-037-26W2/0 CLRD 225 155.2 350.5 350.5 41/16-18-037-26W2/0 MNVL 69.8 106.3 505.7 505.7 41/16-20-034-19W2/0 CLRD 278.9 146.3 262.1 262.1 41/16-20-034-19W2/0 MNVL 132.6 48.8 408.4 408.4 41/16-22-033-08W3/0 CLRD 172.8 191.1 359.7 359.7 41/16-22-033-08W3/0 MNVL -18.3 146.6 550.8 550.8 41/16-22-035-09W3/0 CLRD 153 183.5 386.5 386.5 41/16-22-035-09W3/0 MNVL -30.5 133.8 570 570 41/16-24-035-28W2/0 CLRD 201.8 153.3 344.4 344.4 41/16-24-035-28W2/0 MNVL 48.5 78.4 497.7 497.7 41/16-26-036-04W3/0 CLRD 154.6 151.8 396.2 396.2 41/16-26-036-04W3/0 MNVL 2.8 92.1 548 548 41/16-28-034-08W3/0 CLRD 157.5 181.3 371.6 371.6 41/16-28-034-08W3/0 MNVL -23.8 118.6 552.9 552.9 41/16-29-038-22W2/0 CLRD 266.7 134.1 289.6 289.6 41/16-29-038-22W2/0 MNVL 132.6 121.9 423.7 423.7 41/16-32-036-04W3/0 CLRD 80.7 148.7 436.5 436.5 41/16-32-036-04W3/0 MNVL -68 96.9 585.2 585.2 41/16-32-036-27W2/0 CLRD 222.2 153.6 356 356 41/16-32-036-27W2/0 MNVL 68.6 75.6 509.6 509.6 41/16-33-033-28W2/0 CLRD 194.1 171.6 327.7 327.7 41/16-33-033-28W2/0 MNVL 22.5 93.5 499.3 499.3 41/16-34-032-08W3/0 CLRD 162.2 185.9 368.2 368.2 41/16-34-032-08W3/0 MNVL -23.7 130.8 554.1 554.1 201 41/16-34-035-07W3/0 CLRD 183.8 179.2 329.2 329.2 41/16-34-035-07W3/0 MNVL 4.6 97.5 508.4 508.4 41/16-35-043-26W2/0 CLRD 294.4 141.4 228.6 228.6 41/16-35-043-26W2/0 MNVL 153 173.8 370 370 41/16-36-030-28W2/0 CLRD 206.4 179 377.6 377.6 41/16-36-030-28W2/0 MNVL 27.4 86.8 556.6 556.6 42/13-33-037-01W3/0 CLRD 199.3 143.6 374.6 374.6 42/13-33-037-01W3/0 MNVL 55.7 78.3 518.2 518.2 50/13-22-036-08W3/0 CLRD 186.2 164 318.5 318.5 50/13-22-036-08W3/0 MNVL 22.2 112.5 482.5 482.5 51/04-30-036-26W2/0 CLRD 214.9 116.4 334.1 334.1 61/13-03-035-25W2/0 CLRD 193.5 136.2 361.5 361.5 99/08-13-034-07W3/0 MNVL -18.3 118.9 541 541 202