Authors:B.J.R. Hayes - Dorset Exploration Ltd., CalgaryJ.E. Christopher - Geological Consultant, ReginaL. Rosenthal - Consultant, CalgaryG. Los - Consultant, CalgaryB. McKercher - Inuvialuit Petroleum Corp., CalgaryD. Minken - Maryanne Petroleums Limited, DeWintonY.M. Tremblay - Glyde Resources, CalgaryJ. Fennell - Consultant, CalgaryAdditional Contributors:D.G. Smith - Canadian Hunter Exploration Ltd., Calgary
Mannville Group and equivalent strata comprise the oldest Cretaceous rocks over most of the Western Canada Sedimentary Basin (Figs. 19.1, 19.2) and represent a major episode of subsidence and sedimentation following a long period of uplift, exposure and erosion of older strata (Fig. 19.3). Throughout the text all strata within the generally unconformity-bounded interval are referred to as the Mannville. Precise age determinations are difficult to make because most fossiliferous marine strata are restricted to the northern part of the basin, and index fossils are rare in the continental to brackish sections farther south (Fig. 19.2). Mannville strata blanket the entire basin, ranging from less than 40 m thick in some areas of the plains to more than 700 m thick in the Rocky Mountain Foothills (Fig. 19.4). The section is erosionally truncated along its eastern and northeastern limits. Mannville strata are not mapped as a distinct unit in northwestern Alberta and northeastern British Columbia, where they grade into marine shales that cannot be readily distinguished from younger and older marine strata (Fig. 19.4).
Enormous reserves of coal, natural gas, and conventional and heavy oils are found in the Mannville (Smith et al., this volume, Chapter 33; Hay, this volume, Chapter 32). Coals deposited on extensive low-lying coastal plains are preserved primarily in the present-day foothills and adjacent western plains. Oil and gas are trapped in numerous fluvial and valley-fill reservoir sandstones in the south, and in more regionally extensive shoreline sandstone complexes throughout northern and central regions. The latter category includes the giant heavy oil and oil sands accumulations of Alberta and Saskatchewan (Fig. 19.4).
Geological control for the Mannville is extensive, including abundant petroleum borehole data, outcrop and open pit exposures in the northeastern Alberta oil sands area, and outcrop and coal mine exposures in the Rocky Mountain Foothills. Outcrop exposures are poor along most of the northeastern edge, however, and petroleum borehole data are insufficient for detailed mapping of the interval in the Liard Basin in the extreme northwest.
Because Mannville strata are extremely widespread and heterogeneous, few comprehensive syntheses of the entire group exist. Rudkin (1964) reviewed the Lower Cretaceous of the entire basin, but more recent overview papers have been more geographically limited (e.g., Jackson, 1984).
Some excellent original works of regional scope do exist, however. Stott (1968, 1973, 1982) examined Mannville strata in foothills outcrops and the adjacent subsurface throughout northwestern Alberta, northeastern British Columbia, and the southern Northwest Territories. Glaister (1959; southern plains), Williams (1963; central plains), and Mellon (1967; Rocky Mountain Foothills and plains) described and interpreted Mannville deposits over large areas of Alberta. Subsequent regional work in Alberta has focussed on more restricted stratigraphic intervals and/or areas: McLean (1977, 1982) on parts of the Mannville section in the foothills; Smith et al. (1984) on the "Deep Basin", adjacent to the northernmost foothills of Alberta; Macdonald et al. (1988) on the central foothills; McLean and Wall (1981) on deposits of the mid-Mannville Moosebar Sea across Alberta, and Rosenthal (1988) on related strata of west-central Alberta; Hayes (1986) on the lower Mannville of the southern Alberta plains; Gross (1980) and Putnam (1982) on the east-central plains; and Harrison et al. (1981), Flach (1984) and Keith et al. (1988) on the oil sands of the northeastern Alberta plains.
Christopher (1974) described the Mannville Group of the southwestern part of Saskatchewan, and later synthesized the Mannville depositional history of the entire province (Christopher, 1984). Little has been written on the poorly exposed Mannville section of Manitoba, which was reviewed by McNeil (1984).
Mannville strata make up the second major Cordilleran-derived clastic wedge of the foreland basin, and record the first basin-wide sedimentation (Smith, this volume, Chapter 17). During the Early Cretaceous, accretion of allochthonous terranes in the western Cordillera compressed older miogeoclinal rocks and thrust them onto the continental margin. Stacked thrust sheets loaded the craton edge and caused it to subside, providing accommodation in the foredeep for the huge volume of sediments shed from the upthrusted sheets (Smith, this volume, Chapter 17). Mannville deposition was initiated as these sediments were introduced to the foreland basin, and as base level began to rise in advance of an Early Albian transgression of the Boreal Sea.
Within the foreland basin, several tectonic elements influenced Mannville sedimentation (Fig. 19.1). Three elements - the foredeep, Peace River Arch and Liard Basin - were regional depocentres. Mannville strata thicken abruptly westward from an eastern hingeline toward the foredeep. The Peace River Arch is a block-faulted basement feature that was high during Devonian time, but was a marked low during the Early Cretaceous (O'Connell, this volume, Chapter 28). The thickest Mannville section is preserved where the Peace River Arch and the foredeep converge in northeastern British Columbia (Fig. 19.4). A thick Mannville succession is also found in the fault-bounded Liard Basin, but this area has not been extensively drilled and is documented only in reconnaissance studies (Leckie et al., 1991).
In contrast, the Williston Basin did not subside actively during Mannville deposition. To the west of Williston Basin, the Sweetgrass Arch, a basement feature similar to the Peace River Arch, was uplifted during the earliest Cretaceous and was part of a positive area that was not covered until late in Mannville deposition. The northeastern edge of the Williston Basin was defined by the Punnichy Arch, which formed as the Devonian Prairie Evaporite dissolved in flanking areas to the south and north (Christopher, 1984). Mannville strata thicken north of the Punnichy Arch, where salt solution provided accommodation and abundant clastics were supplied from the Precambrian Shield (Jackson, 1984; Fig. 19.4).
Mannville deposition took place over a profound unconformity surface that truncates strata ranging from lowermost Cretaceous in the foothills to lower Paleozoic at the eastern margin of the basin (Fig. 19.3). Huge valley systems that cut into the unconformity surface influenced sedimentation patterns of the entire Mannville, as discussed below. Although it has been suggested that relief on the unconformity was controlled by tectonic factors (e.g., Christopher, 1984), Cant and Stockmal (1989) considered that differential erosion of dipping Paleozoic carbonate units also may have influenced valley and highland formation across the central plains.
Retun to top
Mannville nomenclature is complex because the strata are geographically widespread and heterogeneous (Fig. 19.2). Everywhere, however, the Mannville lies on the sub-Mannville unconformity. In general, basal Mannville strata are continental, and hence poorly dated, but are generally accepted to be of Aptian age except in the southern foothills, where the Pocaterra Creek Member is pre-Aptian (see Poulton et al., this volume, Chapter 18 for discussion; Fig. 19.2). In the Alberta Plains, where the Mannville lies on Paleozoic carbonates, a highly-variable paleosol or regolith, termed the Deville Member or "detrital" zone, overlies the unconformity in some places (Williams, 1963). In the Saskatchewan Plains, Christopher (1974, 1984) included equivalent strata in the S2 member of the Success Formation, which also comprises thicker, more regionally extensive fluvial deposits made up of distinctive quartz-chert-siderite-kaolin sandstones and mudstones. Both the Deville and Success are considered to predate Mannville deposition, and consequently are mapped in the Atlas as Jurassic units (Poulton et al., this volume, Chapter 18). Some Deville/Success strata may be included in the regional Mannville isopach maps, however, because they can be difficult to distinguish on borehole logs.
An unconformity surface also bounds the top of the Mannville except in northwestern parts of the basin (Fig. 19.2, columns 1-3). This surface lies on top of the Cadotte Member in the Peace River area and at the top of the Cadotte equivalent within the Boulder Creek Formation of the northeastern British Columbia foothills. Strata of the Cadotte and Harmon members and their foothills equivalents should therefore logically be included in the Mannville interval. They are grouped with the Colorado interval in the Atlas because historically, the Cadotte Member has been mapped together with overlying strata as the Peace River Formation in the plains and the Boulder Creek Formation in the foothills.
Ammonites and microfossils in the Spirit River and Gates formations define the upper age limit of the Mannville in western areas (Stott, 1982). The age relations of unconformity-bounded units at the top of the Mannville to the east, such as the Colony Member and Pense Formation (Fig. 19.2), are unclear, because they have not been dated paleontologically. They appear to fit in with Upper Mannville paleogeographic patterns, however, and therefore are included in the Mannville.
Reference logs from subsurface Mannville sections highlight nomenclatural complexities and lithological patterns across the basin (Fig. 19.5). The relations among these sections are presented in the discussions of regional paleogeographic maps and cross sections. A bold line indicates the division between Lower and Upper Mannville in all but the Liard River and Manitoba logs, and a dotted line marks the division in Figure 19.2. Glaister (1959), Williams (1963), Mellon (1967) and Christopher (1974) showed that the Lower/Upper Mannville boundary generally corresponds to an abrupt change in sandstone lithology from a quartz- and chert-rich suite below to a more volcanic and feldspathic composition above. Although more recent work (as discussed below) has shown this boundary to be more gradational than previously thought, a lower/upper subdivision based on lithology is still commonly used and can be applied over most of the basin.
Stratigraphic History and Paleogeography
The complex stratigraphy and paleogeography of the Mannville Group can be characterized in five discrete intervals, reviewed below from oldest to youngest. Each interval records a large number of events into a basin-wide overview, and each paleogeographic map represents a generalized snapshot of those events (see Smith, this volume, Chapter 17, for paleogeographic maps). Interval boundaries are diachronous in the absence of reliable basin-wide time lines. For example, brackish bay environments of the Ostracod/Calcareous interval are significantly younger in the south than in the north (Finger, 1983), but are grouped together on the same paleogeographic map.
Figure 17.3 depicts Cadomin/Gething paleogeography and depositional environments. It represents strata of the Cadomin, Chinkeh and Cut Bank, as well as most of the Garbutt, Gething, Gladstone, Ellerslie, McMurray, Dina, McCloud and lower Mannville units, and the lower part of the Swan River Formation (Figs. 19.2, 19.5).
Along the western side of the basin, a belt of alluvial fans and pediment surfaces flanked the Cordilleran uplift (McLean, 1977). Rivers flowing from this belt fed the basin-axial Cut Bank-Spirit River valley system, which drained northward and was bounded to the east by the Fox Creek and Taber escarpments (Figs. 19.6, 19.7) (McLean, 1977; Hayes, 1986). Conglomerates and coarse sandstones of the Cadomin Formation and Cut Bank Member were laid down on the fans and pediments and in the Cut Bank-Spirit River valley system. As base level rose, great thicknesses of continental and deltaic sediments accumulated in the subsiding foredeep, particularly in the Gething Formation of the Peace River Arch area (Stott, 1973). Sandstones throughout the interval are rich in quartz and chert and poor in igneous detritus, indicating derivation from older, upthrust sedimentary rocks in the Cordilleran source area (Mellon, 1967), or distant source areas in the United States (Christopher, 1974).
To the east, northward-flowing rivers occupying a network of incised valley systems, including the Edmonton and Assiniboia valleys, drained the remainder of the foreland basin and emptied into the northern sea (Jackson, 1984; Christopher, 1984; Putnam, 1989). Fluvial Gething, Gladstone, Ellerslie, Dina, McCloud and associated lower Mannville strata accumulated within the valleys, while the intervening highlands remained emergent. Banerjee and Davies (1988) interpreted much of the Ellerslie fill of the Edmonton Valley to have been deposited under brackish water conditions. Three major deltaic complexes, the Sikanni Chief (Gething Formation), Keg River (Bluesky-Gething), and Fort McMurray (McMurray Formation) formed where the major rivers reached the sea (Stott, 1973; Flach, 1984). The Precambrian Shield supplied quartzose sediments to the eastern valley systems and the Fort McMurray deltaic complex (Harrison et al., 1981). Figures 19.8 and 19.9 illustrate facies relations across the Keg River delta complex.
Figure 17.4 illustrates Calcareous/Ostracod depositional environments and paleogeography. Strata deposited during this interval include: the Ostracod beds and the Calcareous and Cummings members, as well as the upper parts of the Gething, Ellerslie, McMurray, Dina and McCloud units, and the basal part of the Moosebar Formation (Figs. 19.2, 19.5).
Dark calcareous shales, siltstones and lenticular sandstones associated in thin coarsening-upward successions characterize the interval throughout the plains and southern and central foothills. The sandstones are generally siliceous, as in the underlying Cadomin/Gething interval. Thin micritic limestone beds and pelecypod/gastropod/ostracod coquinas also are common (Glaister, 1959; Williams, 1963; Mellon, 1967; Christopher, 1974).
Deposition of Calcareous/Ostracod strata was associated with the early stages of transgression of the Moosebar/Clearwater Sea from the north. Brackish bays advanced southward along the Spirit River, Edmonton, and Assiniboia valley systems, but the major highlands remained emergent (Christopher, 1974; McLean and Wall, 1981). Ostracod/Calcareous strata are generally younger and more continentally influenced to the south (Fig. 19.10; Finger, 1983). Tides had a significant effect on sedimentation within the brackish bay setting (Wanklyn, 1985; Banerjee and Davies, 1988). Precise stratigraphic correlations and environmental interpretations are controversial, but have been addressed by detailed sedimentological and paleontological studies, such as James (1985), Wanklyn (1985), and Banerjee and Davies (1988). Figures 19.10 and 19.11 illustrate some of these correlations and interpretations and are reviewed in more detail in the discussion section at the end of this chapter.
In the Peace River Arch area, fluvial/deltaic deposition of the Gething Formation continued as the influx of Cordilleran-derived sediments kept pace with rising base level. Tongues of marine strata within the upper Gething on the north flank of the Arch in British Columbia are considered to be slightly younger than the Ostracod beds (Duff and Gilchrist, 1981). In Figure 19.10, similar marine tongues at the top of the Gladstone Formation on the south flank of the Peace River Arch are mapped as the lower to middle Moosebar Formation.
Lower Upper Mannville (Glauconitic/Bluesky) Interval
Figure 17.5 illustrates Glauconitic/Bluesky depositional environments and paleogeography. Strata included in this interval are: the Glauconitic, Bluesky, Wabiskaw and Lloydminster, as well as the lower parts of the Moosebar, Clearwater and Dimmock Creek units (Figs. 19.2, 19.5).
Glauconitic/Bluesky strata record the maximum transgression and subsequent early regressive stages of the boreal Moosebar/Clearwater Sea in the southern and central parts of the basin. Sandstones of the interval contain elements of both the underlying siliceous suite and the overlying volcanic-feldspathic suite. In the southern plains, fluvial aggradation began over the Medicine Hat-Swift Current, Kindersley and Wainwright highlands as base level continued to rise. Intervening Calcareous/Ostracod embayments were filled by a flood of coarse clastic detritus from the Cordillera, which was deposited in thin, repetitive, coarsening-upward marine shale/sandstone successions, locally dissected by incised valleys filled with fluvial and estuarine facies. Fluvial and deltaic facies cap the interval (Wood and Hopkins, 1989; Rosenthal, 1988). The northern limit of continental to marginal-marine facies is marked by a complex of progradational marine sandstone bodies, including the Pembina and Hoadley barriers (Rosenthal, 1988). A similar pattern is evident in southwestern Saskatchewan, where fluvial to deltaic facies of the Dimmock Creek Member filled flooded valleys and graded northward into marine sandstones of the Lloydminster Member (Christopher, 1984). To the northeast, fluvial sediments derived from the Canadian Shield were deposited on the Molanosa Highlands.
Open-marine conditions prevailed in more northern areas, as recorded by shallow-shelf deposits of the Clearwater Formation in northeastern Alberta and Saskatchewan (Kramers, 1974; Harrison et al., 1981; Christopher, 1984) and open-marine strata of the Moosebar Formation and Wilrich Member toward the western foredeep (McLean and Wall, 1981). The Wabiskaw and Bluesky are sand-rich units deposited at the base of this marine succession in a variety of transgressive and regressive environments. They are most extensively developed over the Fort McMurray Delta and the Gething Delta complex, and on the flanks of the still-emergent Keg River and Red Earth highlands (Smith et al., 1984; O'Connell, 1988; Ranger et al., 1988).
Recent work has demonstrated that the Moosebar/Clearwater transgression was highly episodic. Several small-scale transgressive and regressive events took place in widely separated areas such as southern Alberta (James, 1985; Wood and Hopkins, 1989), the central Alberta marine sandstone complex (Rosenthal, 1988), Lloydminster (Putnam, 1982), and the Peace River Arch area (O'Connell, 1988). Interfingering of Lower Mannville quartz-chert sandstones with Upper Mannville volcanic-feldspathic sandstones indicates that Cordilleran tectonic events may have altered the sediment supply to the basin, and hence exerted some control on relative sea level (James, 1985; Rosenthal, 1988). Inter-regional correlation of these small-scale events is considered in more detail in the discussion at the end of this chapter, and in Figures 19.10 and 19.11.
Middle Upper Mannville Interval
Figure 17.6 illustrates depositional environments and paleogeography of the middle Upper Mannville interval, which includes the upper Garbutt Formation and lower (Bulwell) sandstone of the Scatter Formation; the Falher, Grande Cache and Torrens members, along with the upper part of the Moosebar Formation and Wilrich Member; the upper Clearwater and lower Grand Rapids formations; the Rex through Waseca members; the upper Dimmock Creek Member and the entire Atlas Member; and the lower parts of the undifferentiated Upper Mannville, Gates and Beaver Mines formations (Figs. 19.2, 19.5). Sandstones in this interval contain significant volcanic and feldspathic components, indicative of Cordilleran tectonic events that exposed volcanic and metamorphic source areas (Mellon, 1967).
Episodic regression of the Moosebar/Clearwater Sea continued after lower Upper Mannville (Glauconitic/Bluesky) deposition. Across the south, fluvial sedimentation is recorded in thick sandstone, siltstone and shale sequences of the foothills (Mellon, 1967), and in repetitive valley incision and aggradation events in the plains (Christopher, 1974, 1984; James, 1985; Hayes, 1986; Wood and Hopkins, 1989; Fig. 19.12). The fluvial regime graded northward into a broad apron of stacked deltaic successions and wave-influenced shorelines across the central Alberta and Saskatchewan plains (Mellon, 1967; Kramers, 1974; Gross, 1980; Harrison et al., 1981; Putnam, 1982; Christopher, 1984; Fig. 17.6). In the extreme northeast, over the former Molanosa Highlands, fluvial quartzose sands derived from the Precambrian Shield continued to accumulate (Christopher, 1984). Thicker stacked prograding successions in the Peace River Arch and foothills areas were reworked along their northern marine margins into continuous high-energy shoreface and beach sandstones and conglomerates (Cant, 1984; Smith et al., 1984; Leckie, 1986, Macdonald et al., 1988; Fig. 19.13).
In the far north, fossiliferous dark shales of the Garbutt, Buckinghorse and Loon River formations record open-marine conditions (Mellon, 1967; Stott, 1982). Shallow-marine sandstone deposits in the Liard Basin are correlated with the middle Upper Mannville interval by ammonites (Stott, 1982).
Upper Upper Mannville Interval
Figure 17.7 depicts the paleogeography and depositional environments of the upper Upper Mannville interval, which includes the entire Notikewin, Mountain Park, McLaren, Colony and Pense units; the uppermost portions of the Grand Rapids, undifferentiated Gates, Upper Mannville, Beaver Mines and Swan River formations; and the uppermost Bulwell Member of the Scatter Formation (Figs. 19.2, 19.5). Uppermost Mannville sandstones contain the same volcanic-feldspathic mineral suite as the underlying interval in the western part of the basin, but are highly quartzose in Saskatchewan and Manitoba.
Fluvial aggradation continued unchanged from the middle Upper Mannville across southern and central Alberta. The two intervals cannot be distinguished except in the central foothills, where the Mountain Park Member lacks the thick coal seams of the underlying Grande Cache Member (McLean, 1982). In the foothills and plains of Peace River, the progradational Notikewin Member was deposited in moderate-energy barrier island and deltaic environments, in contrast to the underlying high-energy Falher shorelines (Smith et al., 1984; Leckie, 1985; Fig. 19.13). Brackish waters transgressed the shallow Pense Basin of Saskatchewan, which then was filled with four, thin, coarsening-upward shoreface successions of the Pense Formation (Christopher, 1974). Much of the upper Swan River Formation in Manitoba comprises restricted-marine facies (McNeil, 1984), and is probably equivalent to the Pense Formation. Deltaic facies of the McLaren and Colony members form the transition between the fluvial and brackish regimes in the Lloydminster area. Some McLaren channels cut into underlying units (Fig. 19.12) and may represent incision and fill events associated with minor relative sea-level fluctuations. To the north, the upper Grand Rapids prograding barrier may have sheltered the Pense Basin from the Boreal Sea, where marine fine clastic deposition continued.
Regional Cross Sections
Six cross sections spanning the entire Western Canada Sedimentary Basin illustrate the stratigraphic relations discussed above. Figure 19.14 shows the lines of section overlain on the Cadomin/Gething paleogeography of Figure 17.3, in order to relate them to specific paleogeographic features.
Section A-A' (Fig. 19.17 left pane and 19.17 right pane) spans the entire Western Canada Sedimentary Basin, from the Liard Basin in the northwest to the Swift Current Highlands in southern Saskatchewan. The five northern wells in the Liard Basin penetrate a thick section including coarse clastics of the basal Chinkeh (Cadomin/Gething interval), Garbutt shales (Ostracod/Calcareous and Glauconitic/Bluesky) and Bulwell sandstones (middle Upper and upper Upper Mannville). South of the Bovie Fault Zone, the Keg River Highlands are covered by thinner Buckinghorse shales (middle Upper and upper Upper Mannville, and post-Mannville).
The Mannville section thickens toward the Peace River Arch area, where coarser continental and shallow-marine clastics that prograded from the west and south dominate. Open-marine shales of the Wilrich Member (Glauconitic/Bluesky) pinch out over the Pembina Highlands, to be replaced by the brackish Ostracod beds and the Glauconitic shallow-marine sandstone complex across the Edmonton Valley. Along the remainder of A-A', the Mannville is thin across the Kindersley and Swift Current highlands, except where it fills valleys on the sub-Mannville unconformity surface.
The westernmost well of B-B* (Fig. 19.15) penetrates the distal edge of the Sikanni Chief Delta (Cadomin/Gething interval). Farther east, Buckinghorse shales lap onto the Keg River Highlands and crop out in wooded swamps of northernmost British Columbia and Alberta (Stott, 1982).
Section C-C' (Fig. 19.16) follows the trend of the Peace River Arch from the foothills to the oil sands. The western wells penetrate the thickest Mannville sections of the basin, where the Peace River Arch and foredeep depocentres converge. Each depositional interval is fully developed: the Cadomin/Gething alluvial fan and deltaic complex (extending through the Calcareous/Ostracod interval); shallow-marine Bluesky progradational facies within the overall Glauconitic/Bluesky transgression, capped by open-marine Wilrich shales; stacked prograding Falher shorelines (middle Upper Mannville), and prograding Notikewin barrier island and deltaic facies (upper Upper Mannville).
Northeastward, the Gething and Bluesky formations lap onto the Red Earth Highlands and the Spirit River Formation grades into undifferentiated, fine-grained marine clastics of the Loon River Formation. At its eastern end, the section intersects the Fort McMurray Delta of the McMurray Formation (Cadomin/Gething and Calcareous/Ostracod intervals), which is overlain by transgressive Wabiskaw sandstones (Glauconitic/Bluesky). Fine-grained marine clastics of the Clearwater Formation grade up into the Grand Rapids stacked prograding barrier deposits of the middle Upper and upper Upper Mannville intervals.
Section D-D' (Fig. 19.18) parallels C-C' but lies south of the Gething delta complex and the Upper Mannville marine and shoreline facies. Thus, in the western half of D-D', a dominantly fine-grained continental section is interrupted only by the brackish Ostracod beds and the shallow-marine deposits of the Glauconitic Sandstone. Coarsening-upward sandstones of the Pembina Barrier are well developed from 16-21-49-13W5 to 11-27-49-8W5, and a Glauconitic incised valley associated with a minor relative sea-level fall is shown in 11-26-53-22W4.
East of the Wainwright Highlands, in the Lloydminster area, stacked continental to marginal-marine facies dominate the entire Mannville section. In the Assiniboia Valley, the McMurray, Clearwater and Grand Rapids formations are difficult to differentiate because they are dominated by brackish-water, low-energy facies south of the Fort McMurray Delta and the Grand Rapids barrier system.
Parallelling C-C' and D-D' in the southern part of the basin, F-F* (Fig. 19.19) traverses thin Mannville sections dominated by continental facies. In the Cut Bank Valley at the western end of the section, the Cut Bank Member represents the eastern limit of lower Cadomin/Gething alluvial fans and braidplains. Brackish-water facies of the Ostracod beds cap the Lower Mannville fill of the Cut Bank Valley, and lap out against the highlands to the east.
The Pense Formation is well developed from the Alberta border eastward, but its coarsening-upward components cannot be resolved at this scale. At the eastern end of the section, sandy fluvial facies lie near the Molanosa Highlands and Precambrian Shield source area.
At the southeastern end of the basin, G-G' (Fig. 19.20) traverses Mannville sections that are entirely continental except for the Pense Formation. The apex of the Moosomin Highlands (6-19-13-32W1) was not covered until Pense deposition, thus hindering correlation of the eastern Swan River Formation with the rest of the Mannville.
Retun to top
The present-day structure of the top-Mannville surface reflects some of the tectonic elements that controlled Mannville deposition (Fig. 19.21). Over most of Alberta the surface dips southwestward, the dip angle steepening toward the foredeep. The Mannville depocentre over the Peace River Arch however, is now a marked positive feature. In Saskatchewan, the Mannville surface dips southward into the Williston Basin; local anomalies are the products of post-Mannville dissolution of Devonian salts (Christopher, 1984). The Sweetgrass Arch trends northeastward from southern Alberta, separating the two regional basins.
Lower and Upper Mannville Isopach Maps
Because of the stratigraphic complexity of the Mannville, only the lower and upper subdivisions can be mapped regionally. The Lower Mannville includes strata of the Cadomin/Gething and Calcareous/Ostracod paleogeographic intervals, and the Upper Mannville groups the lower Upper (Glauconitic/Bluesky), middle Upper, and upper Upper Mannville (Fig. 19.2). The paleogeographic maps are subdivided further because they are more conceptual and do not rely on accurate stratigraphic determinations in each control well.
Lower Mannville Isopach (Fig. 19.22) (Lower Mannville Oil and Gas Fig. 19.23)
Lower Mannville strata are thin to absent over the major highlands on the sub-Mannville unconformity surface, and thicken off their flanks into the Edmonton and Assiniboia valleys. Many of the smaller valleys incising the highlands and secondary to the regional valley systems cannot be resolved at this scale, but are illustrated by regional cross sections A*-A', F-F*, and G-G' (Figs. 19.17 left pane, 19.17 right pane, 19.19, 19.20). A sharp westward thickening in western Alberta marks the Fox Creek Escarpment and the eastern edge of the Spirit River Valley. To the north, lobate clusters of wells outline the Sikanni Chief, Keg River and Fort McMurray deltas, beyond which Lower Mannville marine shales cannot be distinguished from younger strata (see regional cross sections A-A* and B-B*; Figs. 19.17 left pane, 19.17 right pane, 19.15).
Upper Mannville Isopach (Fig. 19.24)
Regional tectonic elements exerted more control over Upper Mannville deposition and resulting isopach patterns. Strata thicken sharply toward the foredeep and Peace River Arch depocentres, where subsidence was greatest, as highlighted by regional cross sections A-A* and C-C' (Figs. 19.17 left pane, 19.17 right pane, 19.16). In the central and southern plains, sub-Mannville valley and ridge systems continued to control isopach patterns, although more subtly, as shown on regional cross sections A*-A', F-F* and G-G' (Figs. 19.17 left pane, 19.17 right pane, 19.19, 19.20). The influence of the Punnichy Arch is expressed as an east-west thin through the Saskatoon area.
At the northern map limit west of 116°ree;W longitude, the Upper Mannville grades to a marine shale succession within the Buckinghorse Formation (section A-A*, 19.17 left pane and 19.17 right pane). To the east, the Mannville top is behind borehole surface casing, and thus has not been determined.
Retun to top
Regional lithostratigraphic correlations within the Mannville are reasonably well understood, but detailed correlations remain poorly documented. This is in part a consequence of the lack of age-diagnostic fossils in the non-marine facies that make up most of the succession, but also reflects the presence of numerous facies changes and internal disconformities. The discussion below attempts to resolve some of the stratigraphic problems, although some of the proposed correlations have not been fully substantiated.
In the southern foothills, the Calcareous Member comprises 50 m of brackish-water facies containing a distinctive ostracod/gastropod/pelecypod faunal assemblage, separating thick continental successions above and below (Fig. 19.10). A fossiliferous black shale with the same faunal assemblage is recognized as far north as Cadomin (Tp 50). North of Ram River, this lithology is overlain by an open-marine shale that includes, and is capped by, a series of regressive coarsening-upward marine sandstones. Farther north, in the Grande Cache area, the fossiliferous shale is absent, and the middle part of the Mannville is a thick, open-marine shale (Moosebar Formation).
The brackish-water shales appear to correlate with two, thin, regressive marine cycles at the base of the Moosebar, implying that Calcareous/Ostracod strata represent a broad, shallow, brackish lake or bay developed behind a barrier island system in northwestern Alberta during the early stages of the Moosebar/Clearwater transgression. Overlying open-marine strata of the Glauconitic/Bluesky interval record the maximum advance and episodic retreat of the Moosebar Sea.
Southern and Central Plains
As described above, the Calcareous/Ostracod and Glauconitic/Bluesky intervals in the northern and central plains comprise basal fossiliferous shale and limestone beds, overlain by a series of regressive, shallow-marine sandstone/shale sequences, locally dissected by incised valleys (Fig. 19.11). The fossiliferous (Ostracod) shales have been noted in core as far north as Township 58 in the west-central plains of Alberta, where they are overlain by open-marine shales of the Wilrich Member. Forty kilometres farther north, the Ostracod shale is absent and the Wilrich rests on marine sandstones of the lower Bluesky Formation (Fig. 19.11). This implies that the Ostracod beds were deposited in a brackish bay behind a barrier island system in north-central Alberta during the initial stages of the Moosebar/Clearwater transgression, the same relationship described above in the foothills.
Correlation Across the Central Highlands
Various stratigraphic schemes have been developed to describe the Mannville in different parts of the basin (Figs. 19.2, 19.5), but it is particularly difficult to correlate those used on either side of the line of highlands in the centre of the basin (Fig. 19.14). As an example, in the Lloydminster area immediately east of the Wainwright Highlands, a complex terminology has been developed to represent abrupt vertical and lateral facies changes. West of the highlands, however, few of the Lloydminster stratigraphic markers can be distinguished, and a simpler stratigraphy is used (see regional section D-D', Fig. 19.18). Thus, our correlation of the upper Dina and Cummings members with the Ostracod beds, for example, requires consideration of the entire succession in both areas.
The central highlands profoundly affected sediment dispersal patterns as well as depositional environments. West of the highlands, Upper Mannville sandstones are composed predominantly of a volcanic/feldspathic suite of minerals derived from Cordilleran volcanic and metamorphic source areas. To the east, the Upper Mannville also includes more quartzose sandstones derived from the Precambrian Shield, and becomes highly quartzose adjacent to the Shield. Near the central highlands, Putnam (1982) interpreted volcanic/feldspathic and quartzose sandstones interfingering in the Upper Mannville as being derived from a variety of western, eastern and southern source areas.
Correlation of Valley-Fill Strata
Incision and subsequent infill of valleys occurred throughout Mannville deposition, ranging in scale from the major valley systems on the sub-Mannville unconformity to small valleys associated with local relative sea-level fluctuations (e.g., Figs. 19.11, 19.12). Strata filling major valley systems generally can be mapped regionally and assigned to well-defined stratigraphic units such as the McCloud Member, Cut Bank Member or Cadomin Formation. The fill of smaller valleys can be mapped only locally, although where several valleys can be associated with a particular incision event, their fills can be informally grouped (e.g., the Glauconitic Formation fill of the Medicine River channels of Rosenthal, 1988).
Extension of local names outside of detailed study areas is difficult to justify because of complex facies patterns and paucity of reliable regional stratigraphic markers. An example is the Sunburst Member, originally defined as a sandstone filling a local valley on the sub-Mannville surface in northern Montana. Subsequent industry usage expanded the Sunburst to include almost any basal Mannville fluvial sandstone in a larger area of southeastern Alberta and north-central Montana. Some workers have even attempted to apply the Sunburst name to brackish facies clearly associated with the Calcareous/Ostracod interval, lying hundreds of kilometres northwest of the original field area. Such extrapolations serve only to obscure understanding of an already complex stratigraphy (see Hayes, 1990, for further discussion).
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We are indebted to Canadian Hunter Exploration Ltd. for a great deal of technical support and general encouragement. Ruth Nixon, John Harkness and Barb Gies in particular provided their considerable skills generously. Peter Putnam and Gordon Williams shared their insights on the Mannville, and their reviews improved this chapter.
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- Banerjee, I. and Davies, E.H. 1988. An integrated lithostratigraphic and palynostratigraphic study of the Ostracode zone and adjacent strata in the Edmonton embayment, central Alberta. In: Sequences, Stratigraphy, Sedimentology: Surface and Subsurface. D.P. James and D.A. Leckie (eds). Calgary, Canadian Society of Petroleum Geologists, Memoir 15, p. 261-274.
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- Christopher, J.E. 1974. The Upper Jurassic Vanguard and Lower Cretaceous Mannville groups of southwestern Saskatchewan. Saskatchewan Department of Mineral Resources, Report 151, 349 p.
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- Duff, P. and Gilchrist, R.D. 1981. Correlation of Lower Cretaceous coal measures, Peace River Coalfield, British Columbia. British Columbia Ministry of Energy, Mines and Petroleum Resources, Paper 1981-3, 31 p.
- Finger, K.L. 1983. Observations on the Lower Cretaceous Ostracode zone of Alberta. Bulletin of Canadian Petroleum Geology, v. 31, p. 326-337.
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- James, D.P. 1985. Stratigraphy, sedimentology and diagenesis of Upper Jurassic and Lower Cretaceous (Mannville) strata, southwestern Alberta. Unpublished Ph.D. thesis, Oxford University.
- Keith, D.A.W., Wightman, D.M., Pemberton, S.G., MacGillivray, J.R., Berezniuk, T., and Berhane, H. 1988. Sedimentology of the McMurray Formation and Wabiskaw Member (Clearwater Formation), Lower Cretaceous, in the central regional of the Athabasca Oil Sands area, northeastern Alberta. In: Sequences, Stratigraphy, Sedimentology: Surface and Subsurface. D.P. James and D.A. Leckie (eds.). Calgary, Canadian Society of Petroleum Geologists, Memoir 15, p. 309-324.
- Kramers, J.W. 1974. Geology of the Wabasca A oil sand deposit (Grand Rapids Formation). In: Oil Sands - Fuel of the Future. L.V. Hills (ed.). Calgary, Canadian Society of Petroleum Geologists, Memoir 3, p. 68-83.
- Leckie, D.A. 1985. The Lower Cretaceous Notikewin Member (Fort St. John Group), northeastern British Columbia: a progradational barrier island system. Bulletin of Canadian Petroleum Geology, v. 33, p. 39-51.
- Leckie, D.A. 1986. Rates, controls and sand-body geometries of transgressive-regressive cycles: Cretaceous Moosebar and Gates formations, British Columbia. American Association of Petroleum Geologists, Bulletin, v. 70, p. 516-535.
- Leckie, D.A., Potocki, D.J., and Visser K. 1991. The Lower Cretaceous Chinkeh Formation: a frontier-type play in the Liard Basin of Western Canada. American Association of Petroleum Geologists, Bulletin, v. 75, p.1324-1352.
- Macdonald, D.E., Langenberg, C.W., and Strobl, R.S. 1988. Cyclic marine sedimentation in the Lower Cretaceous Luscar Group and Spirit River Formation of the Alberta Foothills and Deep Basin. In: Sequences, Stratigraphy, Sedimentology: Surface and Subsurface. D.P. James and D.A. Leckie (eds.). Calgary, Canadian Society of Petroleum Geologists, Memoir 15, p. 143-154.
- McLean, J.R. 1977. The Cadomin Formation: stratigraphy, sedimentology, and tectonic implications. Bulletin of Canadian Petroleum Geology, v. 25, p. 792-827.
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- Mellon, G.B. 1967. Stratigraphy and petrology of the Lower Cretaceous Blairmore and Mannville groups, Alberta Foothills and Plains. Alberta Research Council, Bulletin 21, 269 p.
- O'Connell, S.C. 1988. The distribution of Bluesky facies in the region overlying the Peace River Arch, northwestern Alberta. In: Sequences, Stratigraphy, Sedimentology: Surface and Subsurface. D.P. James and D.A. Leckie (eds.). Calgary, Canadian Society of Petroleum Geologists, Memoir 15, p. 387-400.
- O'Connell, S.C. (this volume). Geological history of the Peace River Arch. In: Geological Atlas of the Western Canada Sedimentary Basin. G.D. Mossop and I. Shetsen (comps). Calgary, Canadian Society of Petroleum Geologists and Alberta Research Council, chpt. 28.
- Poulton, T.P., Christopher, J.E., Hayes, B.J.R., Losert, J., Tittemore, J., and Gilchrist, R.D. (this volume). Jurassic and lowermost Cretaceous strata of the Western Canada Sedimentary Basin. In: Geological Atlas of the Western Canada Sedimentary Basin. G.D. Mossop and I. Shetsen (comps.). Calgary, Canadian Society of Petroleum Geologists and Alberta Research Council, chpt. 18.
- Putnam, P.E. 1982. Aspects of the petroleum geology of the Lloydminster heavy oil fields, Alberta and Saskatchewan. Bulletin of Canadian Petroleum Geology, v. 30, p. 81-111.
- Putnam, P.E. 1989. Geological controls on hydrocarbon entrapment within the Lower Cretaceous Cantuar Formation, Wapella field, southeastern Saskatchewan. Bulletin of Canadian Petroleum Geology, v. 37, p. 389-400.
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- Rosenthal, L. 1988. Wave-dominated shorelines and incised channel trends: Lower Cretaceous Glauconite Formation, west-central Alberta. In: Sequences, Stratigraphy, Sedimentology: Surface and Subsurface. D.P. James and D.A. Leckie (eds.). Calgary, Canadian Society of Petroleum Geologists, Memoir 15, p. 207-220.
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- Smith, D.G., Zorn, C.E., and Sneider, R.M. 1984. The paleogeography of the Lower Cretaceous of western Alberta and northeastern British Columbia in and adjacent to the Deep Basin of the Elmworth area. In: Elmworth - Case Study of a Deep Basin Gas Field. J.A. Masters (ed.). Tulsa, American Association of Petroleum Geologists, Memoir 38, p. 79-114.
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- Stott, D.F. 1968. Lower Cretaceous Bullhead and Fort St. John groups between Smoky and Peace rivers, Rocky Mountain Foothills, Alberta and British Columbia. Geological Survey of Canada, Bulletin 152, 279 p.
- Stott, D.F. 1973. Lower Cretaceous Bullhead Group between Bullmoose Mountain and Tetsa River, Rocky Mountain Foothills, northeastern British Columbia. Geological Survey of Canada, Bulletin 219, 228 p.
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- Wanklyn, R.P. 1985. Stratigraphy and depositional environments of the Ostracode Member of the McMurray Formation (Lower Cretaceous; Late Aptian-Early Albian) in west central Alberta. Unpublished M.S. thesis, University of Colorado, 289 p.
- Williams, G.D. 1963. The Mannville Group (Lower Cretaceous) of central Alberta. Bulletin of Canadian Petroleum Geology, v. 11, p. 350-368.
- Wood, J.W. and Hopkins, J.C. 1989. Reservoir sandstone bodies in estuarine valley fill: Lower Cretaceous Glauconitic Member, Little Bow Field, Alberta, Canada. American Association of Petroleum Geologists, Bulletin, v. 73, p. 1361-1382.
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Authors:S. Creaney - Imperial Oil Resoures Ltd., CalgaryJ. Allan - Imperial Oil Resources Ltd., CalgaryK.S. Cole - Imperial Oil Resources Ltd., CalgaryM.G. Fowler - Geological Survey of Canada, CalgaryP.W. Brooks - Geological Survey of Canada, CalgaryK.G. Osadetz - Geological Survey of Canada, CalgaryR.W. Macqueen - Geological Survey of Canada, CalgaryL.R. Snowdon - Geological Survey of Canada, CalgaryCL. Riediger - The University of Calgary, Calgary
The role of this theme chapter is to familiarize the reader with the current state of knowledge concerning the origin and history of petroleum within the Western Canada Sedimentary Basin. The previous atlas (McCrossan and Glaister, 1964) provided considerable stratigraphic information plus a chapter on formation fluids (Hitchon, 1964). The information contained in the 1964 atlas predated the development of tools that permit the convincing correlation of petroleum fluids to their source rocks and to their thermal regime of origin. In addition, the processes of petroleum alteration via biodegradation and water washing were poorly understood, leaving the origin of Western Canada's oil sands and heavy oil deposits unresolved.
The present contribution provides a summary of the petroleum systems that operate in the Western Canada Sedimentary Basin. It does so from the point of view of petroleum exploration as opposed to a detailed analytical geochemical approach. Thus, summary maps are presented with only sufficient data to illustrate oil-oil and oil-source correlations rather than exhaustive data compilations. These data are located elsewhere in the public literature and are referenced as appropriate.
The authors represent two groups working extensively on petroleum geochemistry in the Western Canada Sedimentary Basin and, as with all science, divergences of opinion do exist. Where these are manifest both arguments are presented. The information herein is drawn from a number of sources, principally Creaney and Allan (1990, 1992), Allan and Creaney (1991), Brooks et al. (1988, 1989, 1990), Osadetz and Snowdon (in press), Osadetz et al. (1991), Riediger et al. (1990 a,b), Riediger (1991) and Deroo et al. (1977).
When analyzing the petroleum systems of any sedimentary basin, especially one whose exploration history is as long as that of the Western Canada Sedimentary Basin, one objective is to understand the geographic and geological distributions of petroleum. Figure 31.1 comprises a pair of histograms showing original in-place conventional oil reserves versus reservoir age for the Western Canada Sedimentary Basin (B.C., Alberta, Saskatchewan). It is this distribution that this chapter seeks to explain. The current state of knowledge of thermal gas-source rock correlation is too poor to make discussion of the geological distribution of gas reserves meaningful in the petroleum system context. Gas occurrence and origin are discussed for certain specific examples wherever the data make this possible.
Formation water geochemistry is not discussed in any detail in this chapter and the reader is referred to Hitchon (1964), and Hitchon et al. (1990) for detailed discussions and more reference material on this topic.
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To facilitate discussion of petroleum in the Western Canada Sedimentary Basin, a petroleum system terminology is used. According to Magoon (1988), "a petroleum system includes all those geologic elements and processes that are essential for an oil and gas deposit to exist." These basic elements include source rock, maturation, migration path, reservoir rock, trap, and seal. Demaison and Huizinga (1991) further refined this concept with their introduction of a genetic classification of petroleum systems. Within this classification the Western Canada Sedimentary Basin is a supercharged, laterally drained, low impedance basin. In actual fact, the basin comprises a number of discrete petroleum systems linked to a number of source rocks. In this chapter each petroleum system is named after the source rock, where possible, and the limits of the system are defined by the extent of migration of petroleum from that discrete source. We also refer to certain systems as being "closed" or "open" systems, which we define as follows. A closed petroleum system is one in which petroleum generated from a particular source generally does not migrate out of rocks of the same age. An example of a closed petroleum system in the basin would be the Middle Devonian reefs of northwestern Alberta, which are sourced exclusively from Middle Devonian source rocks. An example of an open petroleum system would be the Middle Devonian of the Williston Basin (U.S. portion mainly), where Winnipegosis (Middle Devonian) sourced oils are found in Silurian to Mississippian reservoirs. In this case regional seals have been fractured tectonically or via salt collapse structures, thereby "opening" the Middle Devonian system. The terms "open" and "closed" are somewhat imprecise but do allow qualitative comparisons of systems, in terms of their migration style.
Figure 31.2 provides an overview of the source rocks in the Western Canada Sedimentary Basin using the log analysis technique of Passey et al. (1989, 1990). A total of eight marine sources are shown (the Ordovician of the Williston Basin is not shown) and the gas-prone Mannville section is also illustrated.
Although organic geochemical and petrographic terminology is kept to a minimum, certain terms may need explanation. Vitrinite is a coal maceral that is used in the determination of coal rank and organic maturity levels by means of measuring its reflectivity (VR). Kerogen describes the indigenous organic matter of sedimentary rocks, insoluble in common organic solvents, studied using both organic petrological and chemical techniques. Three types of kerogen are defined by atomic hydrogen to carbon (H/C) ratio as Type I (H/C less than 1.4), Type II (H/C 1.2-1.4) and Type III (H/C less than1.0). Rock-Eval pyrolysis is a means of rapidly estimating these values on either kerogen or whole rock through the Hydrogen Index (mg hydrocarbon/g organic carbon). A separate module on this instrument also provides a measure of the total organic carbon content (TOC), the parameter usually used to indicate source rock richness.Tmax, the Rock-Eval temperature (°C) at the point of maximum hydrocarbon evolution during pyrolysis, is a measure of the thermal maturity of the sample, with the oil window typically falling in the range of 430°C to 455°C. Alkanes are saturated (single bonds between the carbon atoms) hydrocarbons. Normal alkanes or paraffins have the carbons arranged in long chains, while the terms cyclic and branched alkanes describe the arrangement of carbon atoms in rings or with side chains. Biomarkers are compounds (commonly polycyclic alkanes) that have structures similar to biological molecules and are commonly diagnostic of the total organic material in a rock. Biomarkers can be used to draw inferences about the depositional environment and to track such processes as maturation, migration, and biodegradation. Typical biomarkers include sterane compounds derived from steroids in living organic matter, and the isoprenoid alkanes, pristane and phytane, derived, at least in part, from chlorophyll. The term odd/even (or even/odd) predominance refers to normal alkane chain lengths and describes the characteristics of paraffin compounds in gas chromatograms. The ratio of odd/even chain lengths can be used to estimate thermal maturity and to draw inferences about the source rock character. All of these terms are discussed in detail in organic geochemical treatises such as that by Tissot and Welte (1984). Many are reviewed briefly in Macauley et al. (1985).
The Ordovician Petroleum System
Source Rocks and Maturity
Ordovician source rocks are known only from the Williston Basin portion of the Western Canada Sedimentary Basin (Osadetz and Snowdon, in press; Osadetz and Haidl, 1989; Osadetz et al., 1989). Sources are described as being generally thin (centimetre to decimetre scale) and laterally discontinuous. They are collectively referred to as "kukersites" and occur sporadically in the Ordovician of Saskatchewan, in the Gunn Member of the Stony Mountain Formation (thin and of unknown lateral extent); Lake Alma Member, Herald Formation; Yeoman Formation; and in the Icebox Member of the Winnipeg Formation (see Norford et al., this volume, Chapter 9). The organic carbon contents of these source rock laminae range up to 35 percent (wt) where pure, with hydrogen indices (HI) commonly > 800 (Macauley et al., 1990). The organic matter is characteristically Type I and composed dominantly of Gloeocapsomorpha prisca (Stasiuk and Osadetz, 1990). Figure 31.3 shows the known occurrence of Ordovician source rocks and their present-day maturity. The definition of mature versus immature zones in Type I kerogen source rocks is somewhat difficult because the kinetic energy spectrum of Type I kerogen is very narrow, resulting in delays of the onset of maturity to around VR = 0.67 percent and oil generation then occurs over a relatively narrow range from 0.67 to 1.10 percent VR (Espitalié, 1986). Using transformation ratios, the oil window can be defined as occurring below present depths of 2950 m in selected parts of southeastern Saskatchewan.
Oil Chemistry and Migration
Ordovician-sourced oils commonly have a characteristic whole-oil chromatogram (Fig. 31.4) that shows reduced amounts of paraffins above C20, a near absence of isoprenoid paraffins and a pronounced odd/even n-paraffin predominance in the C13 - C19 range. The oils are characteristically high quality and low in sulphur content. Sterane (217 and 218 m/z) and terpane (191 m/z) biomarkers are also shown in Figure 31.4 for completeness. All the oils and stains hosted by Ordovician rocks and examined to date (Osadetz et al., 1991) are sourced from Ordovician rocks. In addition, a single occurrence of Ordovician-sourced oil exists outside of Ordovician reservoirs in the Williston Basin (Canada); this occurrence is within the Winnipegosis at Minton, Saskatchewan (Osadetz et al., 1991; Potter and St. Onge, 1991). Thus, the Ordovician is largely a closed petroleum system in Canada, with migration having taken place over relatively short lateral distances and vertically confined by extensive anhydrite seals. Winnipegosis-hosted oil at Minton has migrated vertically via locally developed fractures from the Ordovician into the Middle Devonian Winnipegosis shelf deposits.
To the south, in the U.S. portion of the Williston Basin, faulting and folding have opened the system and connected Ordovician sources to multiple reservoirs (Dow, 1974; Williams, 1974; Zumberge, 1983; Fowler et al., 1986; Leenheer and Zumberge, 1987; Osadetz et al., 1990).
The Keg River/Brightholme Petroleum System
Source Rocks and Maturity
Middle Devonian source rocks have been discussed by several authors (Powell, 1984; Creaney and Allan, 1990; Allan and - Creaney, 1991; Osadetz et al.,1991; Osadetz and Snowdon, in press) and shown to be confined to the Elk Point Basin. Figure 31.5 shows the approximate extent of this basinal source facies with full thermal maturity attained only in southeastern Saskatchewan and northwestern Alberta. In southeastern Saskatchewan, the source facies is a basinal, marine laminite that was deposited coevally with adjacent Winnipegosis reefs. This unit, informally known as the Brightholme member, has organic carbon values up to 46 percent and hydrogen indices up to 800 ±, although more typically a Type II HI of ~615 is observed where immature. The basinal laminites are known to reach 15 m in thickness in Manitoba (Rosenthal, 1987) and to be between 0.6 and 1.0 m thick in Saskatchewan.
In northeastern Alberta, the source facies has been sampled in cores and found to contain up to 15 percent organic carbon with hydrogen indices up to about 440. The sediments are immature in this part of the basin. In the mature, producing areas of Rainbow and Zama, the source has been recognized on logs but not sampled in core (see Fig. 31.2f).
Oil Chemistry and Migration
Several workers have described oil correlations from the Middle Devonian of Western Canada (Clark and Philp, 1989; Allan and Creaney, 1991; Osadetz et al., 1991). At least two oil families are recognized in the Keg River and Muskeg pools in the Rainbow and Zama sub-basins. Oils from the Zama, Shekilie and Virgo pools can be distinguished easily from most Rainbow sub-basin Keg River oils by their triterpane distributions. The latter are unusual in being dominated by 8,14 secohopanes. Possible mixing between the two sources appears to have occurred in Muskeg and some Keg River reservoirs in the Rainbow sub-basin (M.G. Fowler, unpub. data). Despite its proximity to the Zama sub-basin, oil of the Amber area more closely resembles that found in most of the Rainbow sub-basin Keg River reservoirs. The geochemical characteristics of the two principal oil families (Figs. 31.6a, 31.6b) suggest extreme environmental conditions across the floor of the sub-basins, either anoxic (Zama) or saline (Rainbow) conditions.
The occurrence of a laterally restricted source facies between a series of reef pinnacles capped by shale and/or evaporites provides an ideal generation/migration/entrapment situation. Assumed local sources around the pinnacles result in a systematic progression of oil properties from low-gravity, lower maturity oils at the eastern end of the Zama sub-basin to high-gravity oils, condensates and gases as the onset of overmaturity is approached to the west. No evidence exists to date that any Elk Point-sourced hydrocarbons have migrated out of the Middle Devonian in the Rainbow-Zama area and this, therefore, represents a closed system.
The Winnipegosis Petroleum System in southeastern Saskatchewan is also largely closed, because Winnipegosis-sourced oils are confined to adjacent Winnipegosis pinnacles. However, Osadetz et al. (1991) reported the occurrence of these oils in the Mississippian of the Oungre area of southeastern Saskatchewan. They relate this to an absence of overlying Prairie Evaporite, due to dissolution, allowing upward leakage to shallower reservoirs and therefore providing a minor opening of this system. More extensive, structurally related leakage from this system to younger reservoirs has been reported for the U.S. Williston Basin (Osadetz et al., 1990).
The Duvernay Petroleum System
Source Rocks and Maturity
The Duvernay Petroleum System has been extensively described by Stoakes and Creaney (1984, 1985), Creaney (1989), Creaney and Allan (1990), and Allan and Creaney (1991). The Duvernay was deposited as the basinal time-equivalent of Leduc reef growth during the Frasnian and comprises a sequence of dark brown to black, bituminous, slightly argillaceous carbonates interbedded with gray-green, calcareous shales. These sediments are characteristically organic-rich, with total organic carbon (TOC) values of up to 20 percent, and exhibit plane-parallel, millimetre-scale lamination. In the East Shale Basin (Fig. 31.7), the Duvernay Formation overlies platform carbonates of the Cooking Lake Formation with minor discontinuity and is the basinal equivalent of surrounding lower Leduc Formation reefs. The Duvernay thickens northward and eastward up a depositional slope, passing into lithologies more typical of the overlying lower Ireton Formation, which conformably overlies it elsewhere (see Switzer et al., this volume, Chapter 12). Time-stratigraphic markers in the basinal sequence cut obliquely through the top of the Duvernay Formation, indicating the facies-controlled nature of this upper contact (Stoakes, 1980). Basin filling proceeded from east to west, and the top of the Duvernay Formation also rises stratigraphically in this direction. Where the Cooking Lake Formation is absent, as in the West Shale Basin, the Duvernay conformably overlies rocks of similar basinal aspect, referred to as the Majeau Lake Member. The Majeau Lake Member is the basinal equivalent of the Cooking Lake Platform, and as such, predates reef growth. Lithologically it is identical to the Duvernay Formation. Undoubtedly, the Majeau Lake Member contributed hydrocarbons to the Leduc Formation reservoirs, and for convenience it has been grouped with the Duvernay to the west of the Rimbey-Morinville Leduc reef trend for the purpose of this discussion.
The Duvernay and Majeau Lake units represent accumulations under marine, deep-water, low-energy, basinal conditions. Euxinic conditions are suggested by the absence of fauna, preservation of organic material (Type II oil-prone kerogen), colour of the sediment and the presence of framboidal pyrite. Evidence suggests that euxinic conditions existed in water depths on the order of 100 m in the East Shale Basin (Stoakes, 1980). Undoubtedly the presence of anoxic conditions, combined with slow sedimentation rates within this depositional basin, are the main reasons for preservation of abundant organic material in this rich source rock. Euxinic laminites show the highest TOC's (up to 20 percent by weight), with bioturbated dysaerobic or aerobic sediments exhibiting markedly lower organic contents (less than 1.0 percent by weight).
The Duvernay occurs widely throughout Alberta (Fig. 31.7) although much of it is thermally immature. However, a broad arcuate band of the Duvernay is within the oil window, with the most deeply buried portion being overmature.
Oil Chemistry and Migration
Creaney and Allan (1990) described the migration pathways of petroleum sourced from the Duvernay, and Allan and Creaney (1991) provided biomarker data for Duvernay-sourced oils. Duvernay-sourced oils are low in sulphur (less than 0.5 percent) and have pristane/phytane ratios of 1.5 to 2.4 (Fig. 31.8), recording source deposition in normal marine salinities in an oxygen-poor environment. The geochemical characteristics of Duvernay oils are shown in Figure 31.8. As outlined by Creaney and Allan (1990) Duvernay-sourced oils have migrated extensively within the Western Canada Basin. In the area of the Bashaw complex and the Rimbey-Meadowbrook reef chain, Duvernay-sourced oils have migrated into Leduc buildups and then, due to geological connectivity, have passed into overlying Nisku platform carbonates. Pools in the Nisku, such as at Leduc-Woodbend, Golden Spike and Chigwell probably have their origin from the Duvernay.
Stoakes and Creaney (1985) provided a detailed description of hydrocarbon migration in the Woodbend Group, principally along the Rimbey-Meadowbrook reef chain. Oils generated from mature Duvernay source facies have migrated locally into porous and permeable dolomitized Cooking Lake platform margins and Leduc reef buildups. This oil then migrated updip along the platform margin, some accessing overlying reefs such as at Leduc, Redwater, and Acheson, with the possibility of further updip migration until it could access the overlying Grosmont Formation and then possibly to subcrop beneath the Mannville. However no Grosmont Formation bitumen samples analyzed to date have shown evidence of a Duvernay origin (Brooks et al., 1990).
Northwest of the Rimbey-Meadowbrook trend, the Nisku shale basin effectively forms a top seal for the Duvernay system in that direction. Thus, Duvernay oil filled Leduc buildups, spilled into underlying Woodbend platforms, and migrated updip to the platform margin. The nature of platform and reef development in western Alberta resulted in 'stacking' of Leduc platforms and reefs directly on Beaverhill Lake platforms. This local stacking geometry combined with regional tilting allowed Duvernay-sourced oil to spill from Woodbend platforms into stratigraphically older Beaverhill Lake platforms in updip positions. This process continued, with oil ultimately spilling into, and filling, Swan Hills buildups at Swan Hills, Judy Creek, Carson Creek, etc., and the Swan Hills platform margin at Deer Mountain. The remaining excess oil spilled into Middle Devonian Gilwood sands and was prevented from further updip migration only by the stratigraphic pinch-out of these sands at Nipisi and Mitsue.
A similar process of stratigraphically down, but structurally updip, migration occurred on the Peace River Arch, resulting in peak maturity (API 40°) Duvernay-sourced oil occuring in Keg River carbonates as far east as Senex. The Keg River shelf margin on the edge of the La Crete Basin provided the ultimate trap for Duvernay-sourced oil in the Peace River Arch area. To the north of the Peace River Arch the Duvernay (termed the "Muskwa" in that area) is depositionally very basinal (Fig. 31.2e shows the Duvernay/Muskwa in the Rainbow area), and is generally isolated from possible reservoirs (i.e., time-synchronous reefs or underlying platforms). This results in very minor oil reserves attributable to this source north of the Peace River Arch. Brooks and Fowler (unpub. data) have observed differences in biomarkers between the Duvernay and Muskwa. For example, Muskwa extracts and associated oils show a C33 hopane prominence, whereas Duvernay samples show no extended hopane prominence.
Overmaturity in the western part of the Western Canada Sedimentary Basin has produced significant gas generation from the Duvernay. In addition, high present-day temperatures have induced the reaction of interbedded anhydrite with hydrocarbon gases to form hydrogen sulphide which, due to the lack of iron in these carbonate systems, has resulted in considerable reserves of sour gas (Krouse et al., 1989).
The "Nisku" Petroleum System
Source Rocks and Maturity
Chevron Exploration staff (1979) reported the basinal Cynthia Member of the Nisku Formation as the likely source of oils pooled in Nisku pinnacles in the Nisku shale basin. Cores in this particular source rock are not available and therefore corroborating data for source potential in the Cynthia are lacking. TOC's have been reported up to only 2 percent. Thus, the actual correlation of the Cynthia Member to Nisku pinnacle oils is not definitive. This system is therefore given a more generic "Nisku" name pending data corroborating the precise source rock interval for the pinnacle oils. Figure 31.9 shows the occurrence and maturity of Nisku source rocks in the Western Canada Basin.
Oil Chemistry and Migration
The Nisku pinnacle oils of West Pembina show a progressive increase in API gravity from northeast to southwest along the trend, which supports local sourcing from Nisku basinal shales. Allan and Creaney (1991) described oils presumed to be sourced from these Nisku basinal shales. The geochemistry of this oil family is summarized in Figure 31.10. Geochemical data on whole oils are very similar to those for oils from the Duvernay. The terpane data are dissimilar, however, reflecting some differences in the bacterial populations extant during Nisku and Duvernay accumulation (Allan and Creaney, 1991).
Certain Nisku oils in the Stettler and Drumheller areas show characteristics of having been sourced from an evaporitic environment (i.e., pristane/phytane less than1.0, even/odd predominance, etc.) rather than from an open-marine source (Cynthia or Duvernay), and may attest to a source(s) being present in the Nisku evaporitic basin shown in Figure 31.9. In addition, as mentioned earlier, some oils in the Nisku are part of the Duvernay Petroleum System (Golden Spike, Leduc-Woodbend, etc.).
To summarize the Devonian section, the migration of oils in all Devonian systems is shown in Figure 31.11.
The Exshaw-Bakken and Lodgepole Petroleum Systems
Source Rocks and Maturity
Significant, organic-rich, marine, source rock development occurs throughout the Western Canada Sedimentary Basin in the lower part of the Exshaw-Bakken (Devonian-Mississippian) system. Three formations consist of organic-rich, black, basinal laminites: the Exshaw, the Bakken (upper and lower members), and the Mississippian basal Lodgepole formations (see Richards et al., this volume, Chapter 14). The geochemistry of these source rocks has been documented by Webster (1984, Bakken), Leenheer (1984, Bakken and Exshaw), Price et al. (1984, Bakken and Exshaw), Osadetz and Snowdon (in press, Bakken and Lodgepole), Creaney and Stoakes (1987, Exshaw), and Creaney and Allan (1990, Exshaw).
The above authors indicate average TOC's of up to 12 percent for the lower member of the Bakken, 17 to 63 percent for the upper member of the Bakken, up to 5 percent for the Lodgepole, and values up to 20 percent for the Exshaw. In all cases the hydrogen indices suggest a predominantly marine, Type II organic matter. Source rock thicknesses are 3 to 10 m for the Bakken members, less than 10 m for the Exshaw and up to a few tens of metres for the Lodgepole. The distribution and maturity of Devonian-Mississippian sources are shown in Figure 31.12. The actual distribution, regional maturity and richness variations for the Lodgepole source are relatively poorly understood because of a paucity of cores and thus have only been sketched on Figure 31.12. The Lodgepole appears, from extract analysis, to be capable of expelling liquid petroleum at lower levels of maturity than the Bakken, as indicated on Figure 31.12.
Oil Chemistry and Migration
Osadetz et al. (1991) considered the majority of oils in the Williston Basin portion of the Western Canada Sedimentary Basin to have been sourced from Mississippian source rocks. Unlike most previous workers, however, they consider the Lodgepole rather than the Bakken to be responsible for the bulk of the reserves. Bakken-sourced oils are characterized by pristane/phytane ratios greater than 1 whereas Lodgepole oils have a pristane/phytane ratios less than 1, an even/odd paraffin predominance, and a C35 prominence amongst the extended hopanes. Figures 31.13a, 31.13b, 31.13c summarize the geochemical characteristics of Bakken-, Lodgepole-, and Exshaw-sourced oils.
Figure 31.14 shows the currently known extent of petroleum dispersion in the Devonian-Mississippian Petroleum System. According to Osadetz et al. (1991) the Bakken can only be ascribed as source to a limited number of pools (e.g., Roncott, Rocanville and Daly) with the Lodgepole being the source of the majority of Mississippian pools. Impaired expulsion from the Bakken may explain both this observation and the current exploration interest in the Bakken Shale itself as a horizontal drilling target.
The Jurassic and Lower Cretaceous pooled oils of the Rapdan-Battrum trend are also Lodgepole-sourced (Osadetz et al., 1991), as are some Mannville oils of southern Alberta. However, in southern Alberta, other Mannville oils have a strong Exshaw signature and Leenheer (1984), Creaney and Allan (1990), and Allan and Creaney (1991) have suggested the Exshaw as at least a partial contributor to the heavy oils of the Athabasca/Cold Lake/Lloydminster areas.
In the Fort St. John Graben area, Piggott and Lines (1990) ascribed the occurrences of gas in the Wabamun-to-Belloy section as derived from the Exshaw at advanced maturity.
The Doig Petroleum System
Source Rocks and Maturity
The basal, phosphatic and radioactive facies of the Middle Triassic (Anisian) Doig Formation is a prolific oil-prone source rock within the Triassic section of the Western Canada Sedimentary Basin (Creaney and Allan, 1990; Riediger et al., 1989, 1990a). TOC's up to 11 percent and hydrogen indices up to 480 have been reported from peak maturity sections (Riediger et al., 1990a; Riediger, 1990; Creaney and Allan, 1992). The occurrence and regional maturity of the basal Doig source are shown in Figure 31.15. Pooled oils ascribed to this source are also annotated on Figure 31.15. The organic matter type of the basal Doig source facies is typically marine, Type II, consisting of marine algal material and bituminite (Riediger et al., 1990a)
In addition to this important, basal Doig source, other organic-rich intervals occur throughout the Doig and overlying lower Halfway formations in westerly (distal) regions (e.g., in outcrop) of the basin. The underlying, Lower Triassic Montney Formation also contains evidence of source potential, with TOC's up to 5 percent reported (Riediger, 1990; Riediger et al., 1990a). Very high residual TOC values (up to 6.5 percent), in the Upper Triassic Pardonet Formation in outcrop, suggest that this unit likely also generated significant amounts of hydrocarbons as it passed through the oil window. The source potential of these other Triassic units is poorly understood in a regional sense, in part because of the fact that these organic-rich facies are presently preserved only in late mature to overmature regions of the basin.
Oil Chemistry and Migration
Almost all of the oils analyzed to date from Triassic reservoirs are sourced from the basal phosphatic facies of the Doig Formation; however, minor volumes in some Upper Triassic reservoirs are sourced from the overlying Jurassic "Nordegg" Member, and are discussed below. Doig-sourced oils are moderately sulphur-rich (up to 1 percent by weight total sulphur), are generally between 35 and 45° API gravity, and are reasonably distinctive from a biomarker point of view. Diagnostic biomarker characteristics of these oils include pristane/phytane ratios around 1-1.5, high amounts of tricyclic terpanes relative to pentacyclic terpanes, and high diasterane to regular sterane ratios. Figures 31.16a and 31.16b are a geochemical summary of Doig-sourced oils.
Du Rouchet (1985) used aromatic hydrocarbons to suggest the Triassic as a source of the heavy oil deposits of eastern Alberta. This is not supported by more recent biomarker work (Riediger et al., 1990a; Allan and Creaney, 1991; Brooks et al., 1989).
The "Nordegg" Jurassic Petroleum System
Source Rocks and Maturity
The Lower Jurassic of Western Canada contains a highly oil-prone marine source unit, the "Nordegg" Member of the Fernie Formation. The "Nordegg" is probably of Pliensbachian age (Poulton et al., 1990), and consists of dark brown to black, variably phosphatic marlstone and calcareous mudstone with a very high gamma-ray response on geophysical logs. "Nordegg" Member is used in quotation marks to indicate the uncertainty in stratigraphic equivalence of this subsurface unit to the type section of the Nordegg Member in outcrop (see Poulton et al., 1990 for discussion of Jurassic stratigraphy). As indicated by several workers (e.g., Poulton et al., 1990; Riediger, 1991), from west-central to southern Alberta, the "Nordegg" Member undergoes a facies change to a more proximal, brecciated and in part karsted chert- and sand-rich lithofacies, and the oil-source character is progressively diminished (see Poulton et al., this volume, Chapter 18).
Other potential source rocks of Jurassic age include the Toarcian Poker Chip or Paper shales of southern Alberta (Stronach, 1984 reported TOC's up to 4.9 percent; Creaney and Allan, 1992 reported TOC's up to 5.1 percent), and Upper Jurassic (Kimmeridgian age) shales in the Fernie Formation (TOC's up to 4.4 percent reported by Rosenthal, 1989). No detailed geochemical studies of these other units are publicly available, however, and thus their actual hydrocarbon potential remains unknown.
Figure 31.17 shows the distribution and maturity of Lower Jurassic source rocks in Western Canada. As noted above, the presence of oil source rocks south of about 54°N latitude is only implied by published TOC data.
Oil Chemistry and Migration
The geochemical characteristics of "Nordegg"-sourced oils are shown in Figures 31.18a and 31.18b. They are usually extremely sulphur rich (up to 4 percent by weight), and show methyl- and ethyl-cholestane relative abundances characteristic of Jurassic sources (Grantham and Wakefield, 1988). In addition, diasteranes are present in relatively low quantities compared to regular steranes. The 17α (H)21β (H) norhopane is particularly abundant and the C35 hopane shows a relative predominance over the other extended hopanes.
The "Nordegg" rests unconformably on Triassic and older formations, and acts as both source and top seal for some conventional hydrocarbon accumulations (e.g., Rycroft-Charlie Lake, Virginia Hills-Permian Belloy, Cherhill-Mississippian Banff; Figure 31.19). Oils in these pools have properties that reflect the biomarker composition and thermal maturity of the immediately overlying "Nordegg" source rocks, implying minimal lateral migration.
Figure 31.19 is a summary of the known occurrences of "Nordegg"-sourced oil. Considering the richness of the "Nordegg", it is surprising how few conventional oils have unequivocally been correlated to this source rock. The fate of "Nordegg"-generated hydrocarbons is of some debate, even within this group of authors. Some of us (Creaney, Allan, Cole) believe that much of the "Nordegg"-sourced oil is channelled updip in sandier interbeds of the Fernie Group, eventually being trapped in, and contributing a large volume of oil to, the Lower Cretaceous tar sands and heavy oil deposits on the eastern side of the Alberta Basin. Others (Brooks, Fowler, Macqueen, Riediger, Snowdon) note a lack of similarity between biomarker characteristics of the "Nordegg" extracts and the Lower Cretaceous deposits (e.g., Fowler et al., 1989; Riediger et al., 1989, 1990b), and instead suggest that the bulk of the oil generated by the "Nordegg" was not expelled. Thus the "Nordegg" could be a possible target for fractured shale exploration, similar to the Bakken Formation in the Williston Basin.
The Mannville Petroleum System
Source and Maturity
The earliest deposits of the foreland basin are dominated by deltaic/coastal plain sedimentation, and are characteristically coal rich. Welte et al. (1984) provided an excellent geochemical description of this part of the section in the Elmworth area. Furthermore, these coals are mined at outcrop in the Disturbed Belt and their petrographic composition is well described (Cameron, 1972; Kalkreuth, 1982). The coals are notably low in liptinite and commonly rich in inertinite (see Smith et al., this volume, Chapter 33). Pyrolysis analyses shows Mannville sediments to contain primarily Type III kerogen, which led Welte et al. (1984) to conclude that they are very potent gas sources, particularly at the advanced levels of maturity found in the Deep Basin (Kalkreuth and McMechan, 1988). Welte et al. (1984) further suggested that the 17 TCF of proven and probable natural gas in low-porosity Lower Cretaceous sands of Western Canada's Deep Basin was largely generated from local, high-maturity coals and migrated into adjacent low-porosity and permeability sands. Masters (1979) had earlier proposed that these gases are hydrodynamically trapped, given that the sands are water filled updip from the "tight gas sands."
TOC values in associated shales are commonly below 2 percent, with very low hydrogen indices (Moshier and Waples, 1985). However, the presence of locally restricted, delta-plain and lacustrine shales containing concentrated amounts of liptinites or sapropelic material cannot be discounted. Hence, localized oil or condensate with commercial potential may exist. Figure 31.20 is a maturity map of the Mannville based on coal vitrinite reflectances and compiled from a variety of sources.
In the very northern portion of the Western Canada Sedimentary Basin, the Mannville delta-fronts grade into prodelta and ultimately distal, marine sediments that develop oil-source potential. This has been observed in the Northwest Territories in the Slater River shale at the East Mackay B-45 well (Feinstein et al., 1988).
The Mannville section in Western Canada performs a double role relative to petroleum distribution. The Mannville Petroleum System consists largely of internally sourced and pooled gas (highly mature coal gas in the west grading to bacterial gas in eastern Alberta). In addition the basal Mannville sand-prone section has acted as a "collector" for prodigious volumes of oil (see Hayes et al., this volume, Chapter 19) from pre-Mannville source rocks. There are currently two schools of thought on the origin of the vast reserves (~1.8 trillion barrels) of heavy oil in the Mannville-Grosmont reservoirs and both schools are represented within the authorship of this chapter.
Creaney and Allan (1990), Allan and Creaney (1991), and Creaney and Allan (1992) consider these huge deposits to be a mixture of oils leaking from the immediately underlying section with principle contributions coming from the Jurassic ("Nordegg" and possibly younger Jurassic) as well as the Mississippian (Exshaw/ Bakken). In addition, there are other subcrops that are connected to the Mannville; for example, Nisku and Triassic (very limited) that could, on geological grounds, have leaked oil to the Mannville, but no geochemical evidence is known to support this. In contrast, Brooks et al. (1988, 1989, 1990) analyzed samples from each heavy oil deposit and, recognizing the strong similarity amongst them, concluded that they must belong to a single family with a unique source. To date this source has not been identified. Biomarker studies indicate no clear-cut correlation between conventional oils and their known source rocks and these bitumen deposits (Brooks et al., 1990). Figure 31.21 summarizes the occurrence of heavy oils in Western Canada and suggests one possibility for their source and migration from Jurassic and Mississippian sources.
The Colorado Group Petroleum System
Source and Maturity
The Colorado Group of Late Cretaceous age is a thick, marine shale and siltstone succession that contains several oil-source horizons (see Fig. 31.2a; and Leckie et al., 1990). In the southern part of the basin, two principal effective source zones are the Second White Speckled Shale (Cenomonian/Turonian) and the Fish Scales Zone (Albian/ Cenomanian). Both contain marine, Type II organic matter with TOC's up to 12 percent and hydrogen indices up to 450 where immature (Allan and Creaney, 1988). Between the condensed sections are other effective marine, though less rich, source intervals, where TOC's are in the 2 to 3 percent range and hydrogen indices range up to 300. In the central part of the basin, the younger First White Speckled Shale condensed section (Santonian) becomes more organic-rich and develops source potential. This is normally less prominent on natural gamma-ray logs than the older condensed sections, but has source quality characteristics similar to the older Second White Speckled Shale.
Colorado Group shales are mature in the most westerly part of its zone of occurrence, adjacent to the Disturbed Belt (see Fig. 31.22). Peak maturity of the Second White Speckled Shale and the Fish Scales Zone lies close to the Disturbed Belt in the southern part of the basin. Passing northward, deeper maximum burial causes these two source zones to trend toward overmaturity and the First White Speckled Shale then becomes mature along the basinal axis. In central Alberta, the maturity contours swing east-west and run into the Disturbed Belt. Thus there is a broad area from central Alberta north to outcrop where the Colorado Group is immature. Very low maturities are present throughout Saskatchewan, and the condensed sections discussed above have been locally classified as oil shales (Macauley, 1984a, b; Macauley et al., 1985). To date, organic enrichment has been observed to occur at the base of the Shaftesbury (northern Alberta; Leckie et al., 1990) and at the Base of Fish Scales, Second and First White Speckled Shales (see Fig. 31.2a).
Oil Chemistry and Migration
Without exception, all oils pooled in Viking and all younger sands are sourced from the Colorado Group shales. These are sweet, high quality crude oils, with sulphur contents usually less than 0.4 percent by weight.
Steranes of Colorado Group-sourced oils consistently have a C28>C29>C27 relative abundance (Fig. 31.23), as do steranes in organic extracts of the shales themselves. The transition from the C29>C27>C28 relative pattern of all older source rocks and their oils to the Colorado Group distribution occurs in Albian rocks and has been documented in core extracts (Creaney and Allan, 1992). The change in sterol abundances is likely related to the emergence of coccolithophorids and silicoflagellates as prominent contributors to the steroidal budget of marine muds (Grantham and Wakefield, 1988). Indeed, the predominance of the C28 steranes appears to be a worldwide phenomenon characteristic of Late Cretaceous marine source rocks.
As previously stated, all oils found in Viking-Belly River reservoirs are sourced from the Colorado Group. Furthermore, Colorado Group-sourced oil has not been documented in any Mannville or older sediments. Thus, there appears to be a basin-wide, hydraulic barrier between the Viking-Belly River reservoirs and Mannville and older sediments. Stratigraphically this corresponds to the Albian Lower Shaftesbury/Joli Fou formations (Allan and Creaney, 1988; Creaney and Allan, 1990). The lack of any correspondence in either degrees of oil alteration or geographic distribution of altered oils above and below these shale formations strongly supports the concept that this level represents an oil, water and perhaps gas permeability barrier.
Viking oils, which are widespread across southern Alberta and eastern Saskatchewan, have been sourced from mature Cenomanian-aged shales of the Colorado Group adjacent to the foothills of southern Alberta.
Cardium oils lie in traps localized at or below erosion-transgression surfaces, as described by Plint et al. (1986) and Walker (1988). The major Cardium accumulation is the giant Pembina Field, which lies in regressive sands situated below the transgressive conglomerates on the E5 surface (Plint et al., 1986). The bulk of the oil is peak maturity liquid derived from the Second White Speckled Shale some considerable distance downdip from the reservoirs (Allan and Creaney, 1988). Similar oil is found at Cynthia/Pembina, Keystone, Carrot Creek and Willesden Green. A number of Cardium pools occur in sandstone associated with surfaces other than the E5. Examination of their geochemical properties (maturity and biomarker profiles) suggest that they are pooled close to their sources, and are most likely derived from shales adjacent to their reservoir sands. The maturities of these oils (Kakwa, Garrington and Crossfield fields, for example) are similar to the maturities of closely adjacent shales.
Oils in Belly River channel and shoreline sands in central-southern Alberta are commonly peak-maturity liquids and are very similar to oils in underlying Cardium pools. Quantitatively, total reserves represent only a small fraction of the Cardium reserves. They can be considered as a small amount of "overspill" oil from the Second White Speckled Shale, which failed to access Cardium sands. Thus, a considerable cross-stratal component exists for the secondary migration pathway of Belly River oils, coupled with a significant amount of updip migration once the oil accessed channel sand. Figure 31.24 summarizes migration pathways in Colorado Group reservoirs.
Fuex (1977) published isotope analyses for several Western Canada gases, including some from the large (3 TCF) gas pool at Medicine Hat in the Milk River Formation. This gas is biogenic (generated by bacterial decay rather than thermal degradation), and was probably sourced from adjacent Colorado Group mudstones (including the First White Speckled Shale condensed section). Much of the very dry gas (methane only) of eastern Alberta is probably of this origin. This has an interesting implication for petroleum migration because it begins to fill trap volume almost immediately after reservoir deposition, which could leave certain traps full of gas prior to the later arrival of oil. This oil would then fail to "see" the trap and might be facilitated in it's long distance lateral migration.
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Milner et al. (1977) outlined the processes that can alter or degrade an accumulation of oil. Two of these processes have had a significant impact on the original reserves of the Western Canada Sedimentary Basin:
Biodegradation. Biodegradation is the action of microbes on accumulated oil, resulting in the oil's degradation to heavy oil. Degradation is caused by the incursion of oxygenated meteoric water from outcrop areas into reservoirs and is a combination of aerobic and anaerobic microbial processes. Biomarker evidence shows that several different biodegradation pathways must be occurring in these deposits (Brooks et al., 1988, 1989). In Western Canada this has happened to approximately 98 percent of the oil originally in place as conventional reserves and has produced the giant oil sands deposits at Buffalo Head Hills, Peace River, Athabasca-Wabasca, Cold Lake and Lloydminster. These occur in Lower Cretaceous (Mannville) and Carboniferous and Devonian ("carbonate triangle") intervals.
Figure 31.25 is a map of oil alteration (via biodegradation) and formation water salinity in the Mannville of Western Canada. It is the excellent reservoir quality and continuity of the basal Mannville section that has allowed both the long-distance migration of oil and the considerable ingress of meteoric water required for biodegradation. Oils that occur in subcrops beneath the Mannville (for example, Grosmont, etc.) are also biodegraded where fresh water has travelled down from the Mannville. Figure 31.26 is a montage of geochemical data showing sequential biodegradation of Mannville oils. Biodegradation is most severe in areas of the Athabasca Deposit, with a reduction in intensity to Peace River (where some n-alkanes remain preserved) and to Lloydminster (where the isoprenoids pristane and phytane are still preserved). It is interesting to note that biodegradation is largely confined to the Mannville and adjacent subcrops, with only minor degradation reported from younger shallow Viking sands as well as older rocks without subcrop access to the Mannville. This attests to the laminar nature of freshwater incursion at Mannville outcrop and argues against wholesale cross-formational water flow access (Garven, 1989).
Thermal Alteration. A number of reservoirs in the western part of the basin contain significant quantities of reservoir bitumen (a black, solid carbon-rich residue) plus a very light oil and significant associated and dissolved gas. An example would be the Brassey Field (Triassic Artex Sand pool), which occurs very close to the mature-overmature transition. The association of these petroleum products and the maturity regime of the reservoir conform to a model of early emplacement of an oil-only phase with subsequent thermal elevation and in-reservoir cracking of oil to gas and bitumen.
Deasphalting. This is the process of co-mixing petroleum products (commonly oil and gas) with a resulting precipitation of asphaltenes. This material appears as soft, black, solid material occluding reservoir porosity. In examples from the Rainbow area of northern Alberta, precipitated asphaltene is clustered at the oil/water contact. In the Leduc-Woodbend reef the trap probably only contained oil originally at the reef crest. Later ingress of gas precipitated asphaltene and pushed the oil down the reef, resulting in the present-day occurrence of precipitated asphaltene in the gas cap porosity.
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Timing of Petroleum Generation
Several authors have developed burial history profiles for the Western Canada Sedimentary Basin (e.g., Deroo et al., 1977; Creaney and Allan, 1990; Issler et al., 1990). Figure 31.27 is a typical burial history profile representing most of the Western Canada Sedimentary Basin. The principle phase of oil generation was during the Late Cretaceous - Early Tertiary Laramide burial, although there may, in certain areas, have been minor oil generation prior to this time.
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The Western Canada Sedimentary Basin contains at least nine active petroleum systems driven by the following source rocks:
- Ordovician - marine kukersites of the Stony Mountain, Herald, Yeoman and Winnipeg formations
- Middle Devonian - basinal marine laminites of the Keg River/Winnipegosis formations
- Upper Devonian - basinal marine laminites of the Leduc-equivalent Duvernay and Cooking Lake-equivalent Majeau Lake formations
- Upper Devonian - basinal laminites of the Cynthia Member of the Nisku Group
- Uppermost Devonian and lowermost Mississippian - the basin-wide marine mudstones of the Exshaw/Bakken formations as well as the more locally developed shales in the Lodgepole Formation
- Middle Triassic - the marine phosphatic siltstones at the base of the Doig Formation
- Lower Jurassic - the marine lime muds of the "Nordegg" Member of the Fernie Group
- Lower Cretaceous - the continental coals and carbonaceous shales of the Mannville Group
- Upper Cretaceous - the marine mudstones of the Colorado Group, principally the First and Second White Speckled Shales and the Fish Scales Zone
In general, these source rocks are thermally mature only in the more deeply buried western half of Alberta and the southeastern corner of Saskatchewan (northern rim of the Williston Basin).
The Mannville has acted as a major regional collector for oil draining from thermally mature, pre-Mannville source rocks. This has resulted in the focussing of some 1.8 trillion barrels of oil into the super-giant accumulations at Peace River, Athabasca-Wabasca, Cold Lake and Lloydminster. However, significant ingress of meteoric water at Mannville outcrop has allowed biodegradation to proceed and the oil is biodegraded to heavy bitumen. In fact only approximately 30 billion barrels (1.8 percent) of oil that was generated and migrated from the pre-Mannville section remains conventional. This confirms the supercharged, high efficiency, low impedance designation of Demaison and Huizinga (1991).
In contrast, the Colorado section, above the Joli Fou shale and its equivalents, has been isolated (with respect to oil migration) from the underlying Mannville and pre-Mannville section. The updip pinchout of Cardium and Viking sands has precluded the ingress of fresh water and therefore biodegradation is minimal in the Colorado petroleum system. Thus, of the approximately 12 billion barrels of oil in this system, 100 percent is considered to be conventional. In this respect the Colorado system would be classified as a supercharged, high efficiency, high impedance system.
Figure 31.28 presents the same conventional reserves data shown in Figure 31.1, with colour coding according to the source rock responsible for the reserves.
Advanced maturity in the western portion of Alberta and in British Columbia is responsible for significant quantities of thermal gas generated in all petroleum systems (with the exception of the Williston Basin-confined Ordovician system). In addition, the immature eastern portion of Alberta contains significant biogenic methane in a number of reservoirs.
It should be stressed that the analyses presented here represent only a regional overview of the major petroleum systems. Local variations on this general scheme do occur, and more work should refine this overall model. Also, although the source(s) for the oil sands/bitumen/heavy oils has been resolved to the satisfaction of some of us (Creaney, Allan, Cole) the rest of us await additional evidence and documentation of source intervals in the basin before assuming an entrenched position regarding this most important oil-source correlation in the Western Canada Sedimentary Basin.
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The authors would like to thank fellow staff and management at Imperial Oil Resources Limited and the Institute of Sedimentary and Petroleum Geology for encouragement and technical support during the preparation of this chapter, and for permission to publish.
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- Allan, J. and Creaney, S. 1988. Sequence stratigraphic control of source rocks: Viking-Belly River System (Abstract). In: Sequences, Stratigraphy, Sedimentology; Surface and Subsurface. D.P. James and D.A. Leckie (eds.). Canadian Society of Petroleum Geologists, Memoir 15, p. 575.
- Allan, J. and Creaney, S. 1991. Oil families of the Western Canada Basin. Bulletin of Canadian Petroleum Geology, v. 39, p. 107-122.
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