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Meander Belt Entrapment of Hydrocarbons, Campbell-Namao Field, Alberta
By
Ralph W. Edie1 and John M. Andrichuk1
Search and Discovery Article #20029 (2005)
Posted July 27, 2005
1Independent geologists, 504 Fording Place, 205 – 9 Avenue S.E., Calgary, Alberta, Canada T2G 0R3 (telephone: 403-269-6084)
Abstract
At Campbell-Namao Field, near Edmonton, Alberta, Lower Cretaceous uppermost Ellerslie Member hydrocarbon-bearing quartz sandstone reservoirs include sandstone bodies with markedly different shapes and origins as follows:
(1)
approximately 20 metre-thick sandstone
bodies, with an areal extent as great as 518 hectares (2 square miles), that
exhibit “fining-upward” response on electric logs and are interpreted as 
point
bar sandstones along a river meander belt.
(2) thin sheet sandstones (5 metres thick) of relatively uniform thickness and widespread areal extent, interpreted as being of marine origin.
Within the interpreted meander belt, there are numerous point bar sandstone
bodies, some (but not all) of which contain stratigraphically entrapped
hydrocarbons. A roof-seal is provided by a widespread shaly bed. Updip, lateral
and downdip sealing is provided by shale-filled channels or oxbows that locally
completely surround the point bar sandstone bodies.
Within the interpreted meander belt, 14
shale-filled channels were intersected in boreholes. In the central portions of
the shale-filled channels, the compacted shale filling, as measured on electric
logs, varies from 14.6 to 23.5 metres (48 to 77 feet). Gas and oil were
entrapped in compartmentalized reservoirs and each compartment (point bar or
point bar remnant) is characterized by a measurably different subsea gas-oil or
oil-water contact. Maximum gross pay thickness is 27.4 metres (90 feet).
In several parts of the meander belt,
interpreted point bar sandstones are mainly water-bearing: only point bar
sandstones or remnants of point bar sandstones that are completely surrounded by
shale-filled channels appear to trap commercial quantities of hydrocarbons.
Hydrocarbon entrapment within the thin sheet sandstones is caused by:
(a) updip and lateral facies change from permeable sandstones to shaly beds;
(b) updip and lateral truncation of the thin sheet sandstones by shale-filled deeply entrenched meandering river channels along the concave downdip edge of the meander belt.
Within the field area, the hydrocarbon-bearing portion of the thin sheet
sandstones cover an area of 2331 hectares (9 square miles). However, the
water-bearing segments of these sandstones extend over a much greater area,
beyond the field limits. Total production at Campbell-Namao Field, from both
point bar and thin sheet sandstone reservoirs, to the end of March 2002, is 3183
x 106m3 (113 Bcf) and 922 x 103m3
(5.8 million barrels) of 33°A.P.I oil.
In central Alberta, upper Ellerslie meander belts are mapped from electric logs
with relatively sparse well control. In exploratory drilling, along those
meander belts, hydrocarbon reserves similar in size to those in productive point
bar sandstones at Campbell-Namao Field (i.e. 5.8 Bcf gas and 258,000 bbls oil
per square mile) can be expected. Moreover, if “bright spot” seismic technology
to map upper Ellerslie Member gas accumulations (with or without associated oil
columns) can be improved, it should be possible to attain almost 100% success in
exploratory drilling along known upper Ellerslie meander belts.
The exploration procedure outlined
herein applies to meander belts of various ages world-wide, provided that: (1)
the point bar sandstones retain their porosity and permeability; (2) source
rocks at sufficient depth and temperature are available to generate
hydrocarbons; and (3) the point bar sandstones have a roof-seal.
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IntroductionAt the Campbell-Namao Field near Edmonton, Alberta, natural gas and petroleum occur in compartmentalized sandstone reservoirs associated with a Lower Cretaceous river meander belt. The updip and downdip limits of a segment of that meander belt are shown in Figure 1a. The producing wells within the Campbell-Namao Field during the early stage of field development are shown in Figure 2. The reservoir sandstones occur in the upper part of the Ellerslie Member of the Mannville Group at a depth of 1130 metres (3700 ft.). Within the meander belt, the hydrocarbon pools have a bottom water drive. Most of the producing gas and oil wells have reached their economic limit of production and are now abandoned. No secondary recovery scheme for producing additional oil has been attempted. Total production to the end of March 2002 is 3183 x 106 m3 (113 Bcf) gas and 922 x 103 m3 (5.8 million barrels) of oil. The discovery well for the Campbell-Namao Field was Redwater Leaseholds Campbell 1-28-54-25 W4M (Figure 2). The well was completed as an Ellerslie Member oil well in 1949, and it yielded 33º A.P.I. oil. During early field development, because of a lack of market for the natural gas, gas associated with produced oil was flared. The Alberta Oil and Gas Conservation Board (now Alberta Energy and Utilities Board) attempted to reduce gas flaring by instituting severe production penalties for high gas-oil ratio wells. The gas and oil wells on production at the Campbell-Namao Field 17 years after the initial discovery are shown in Figure 2. In 1966, upon recommendation of the authors, Oakland Petroleums Ltd., drilled the 12-25-54-25 W4M well which resulted in discovery of a new oil pool. This oil pool had a different subsea oil-water contact from that at the Namao pool to the north (Figure. 2), and with continued drilling, Oakland developed a major extension of the Campbell-Namao gas and oil field covering 2395 hectares (9¼ square miles) (Figure 2). From this extension, Oakland Petroleums Ltd. and successor companies produced 380 x 103m3 (2.39 million barrels) of crude oil and 1518 x 106m3 (53.9 Bcf) of gas (i.e., 258,000 bbls. oil and 5.8 Bcf gas per square mile). During the extension development, at least one of the authors performed the well-site geological work at every well drilled by Oakland Petroleums Ltd. and recommended:
The purpose of this paper is to document
meander belt entrapment of hydrocarbons in a gas and oil field with
relatively close well spacing (mainly 16 to 32 hectare spacing). Within
the meander belt, hydrocarbons are entrapped in fining-upward,
20-metre-thick sandstone bodies, interpreted as of The mapping techniques outlined herein may be of interest to exploration personnel worldwide involved in the search for stratigraphically entrapped hydrocarbons in sandstone-shale sequences.
Field Work by the AuthorsAt the wellsite, collection of drill cuttings was carefully supervised at 5-foot or 2-metre intervals and the freshly caught wet cuttings were immediately examined with a binocular microscope. Ellerslie gas-bearing sandstones were clearly recognized by the presence of scattered droplets of gassy brown oil when fragments of the reservoir sandstone were broken with tweezers. Similarly, oil saturated sandstone, characterized by droplets of gassy brown oil in every pore, was identified. Finally, the first appearance of water-wet sandstone, lacking droplets of gassy brown oil, was indicative of the oil-water contact. Thus, the approximate subsea elevation of the gas-oil and oil-water contact at each well was determined from microscopic examination of the wet drill cuttings prior to logging. A more precise subsea elevation of the gas-oil and oil-water contact at each well generally was determined from examination of the sonic and resistivity logs. At Campbell-Namao Field, induction resistivity logs of gas-bearing Ellerslie Sandstone commonly register 12-30 ohm-metres resistivity and oil-bearing sandstones commonly register 8-12 ohm-metres resistivity. Water-bearing sandstones, unless deeply invaded by fresh water based drilling mud filtrate, exhibit less than one ohm-metre resistivity. The oil-water contact at each well was arbitrarily drawn at 4 ohm-metres resistivity. At most wells, the only porosity log run was the gamma ray-sonic so that a combination of neutron-sonic or neutron-density log was not available to determine “cross-over” presence of gas. In most instances, drillstem tests were undertaken to confirm the microscopic and log interpreted gas-oil and oil-water contacts. It should be pointed out that in clean reservoir sandstone, the gas-oil and oil-water contacts can be precisely determined from examination of the sonic and induction resistivity logs. However, this determination is less certain where the gas-oil or oil-water contact coincides with thin shaly beds within the reservoir sandstone.
StratigraphyThe term Ostracode zone was first used by Hunt (1950) who described the zone as calcareous fossiliferous black shale, approximately 45 feet thick. Loranger (1951) also described the Ostracode zone and its contained fossils, which include several species of ostracodes, including Metacypris persulcata, pelecypods, and gastropods. From her paleontological studies, Loranger considered the Ostracode zone to be of brackish water origin. Holmden et al. (1997), in isotope studies of Ostracode zone fossils, concluded that the Ostracode zone was mainly a fresh water deposit, perhaps similar to deposits in the present-day Lake Maracaibo, Venezuela. The Blairmore “Calcareous” Member mapped by Glaister (1959) in the foothills of southwestern Alberta is considered by him to be equivalent to the Ostracode zone. Rudkin (1964) states that although the Ostracode zone was originally described (by Loranger) as a faunal zone, it is also a readily mappable lithologic unit. In parts of the Edmonton area, the Ostracode zone, which directly overlies the Ellerslie Member, is considered to be a mainly fresh to brackish water embayment or lake deposit near the edge of the southerly transgressing Boreal sea (McLean and Wall, 1981, Figure 5). In the Campbell-Namao field area, the Ostracode zone consists of two beds (comprising dark brown to black argillaceous limestone or calcareous shale containing shells of gastropods, pelecypods, and ostracodes), characterized by high resistivity on electric logs, separated by a black fissile shale bed (Figure 3). West and southwest of the Campbell-Namao Field, the lower part of the Ostracode zone changes facies to a porous and permeable sheet sandstone which is the reservoir for the Alexander and Big Lake gas fields (Figures 1a and 4). As shown in Figure 1a, the gas-water contact at the Alexander and Big Lake gas fields is –473.7 m and –502.6 m, respectively. The water-bearing parts of the Ostracode zone sandstone bodies, lying downdip to the southwest of the Alexander and Big Lake gas fields, were readily mapped by the authors because the SP, gamma ray, and resistivity logs show clean porous sandstone with very low resistivity. The well control is sufficient to map the extent of the sandstone bodies with a fair degree of precision. It should be pointed out that in the Edmonton area, inconsistencies exist in the geological literature concerning correlation and nomenclature of Ostracode zone members. For example, although Mason (1969b) correctly places the reservoir sandstone at Big Lake Gas Field within the Ostracode zone, at Alexander Gas Field, Mason (1969a) incorrectly places the reservoir sandstone within the Basal Quartz (Ellerslie) member. Similarly, at Alexander Gas Field, Jackson and Bournes (1968) also incorrectly place the Lower Ostracode zone sandstone within the Ellerslie Member.
According to Jackson and Bournes (1968),
the Descriptions of the Alexander and Big Lake gas fields, including gas pay isopach maps, were published by Mason (1969a and 1969b). Although Mason (1969a and1969b)described the lower Ostracode Sandstone reservoirs at Alexander and Big Lake gas fields as quartzose sandstones, detailed examination of cores from Midwestern Gas Alexander 10-23-56-1 W5M and Hewitt Big Lake 11-34-53-26 W4M by one of the authors (Edie) shows that these sandstones are composed of approximately 80% quartz grains (with quartz crystal overgrowths) and 20% white to dark gray well rounded chert grains. The sandstone composition is thus similar to Ellerslie equivalent productive Basal Quartz sandstones in the Bantry – Alderson – Taber areas (referred to as “BAT” sandstone) and described by Arnott, et al. (2000) The grain size of the lower Ostracode zone sandstone at Alexander and Big Lake gas fields varies from fine-grained to medium-grained (Wentworth scale) and is distinctly coarser than the underlying upper Ellerslie quartzose sandstones near Edmonton, Alberta. In the cores examined, a few wispy planar to wavy paper-thin dark gray shale partings dip at angles of 5 to 20º. The SP log response of the reservoir sandstone at some of the wells at Alexander and Big Lake fields clearly exhibit a “coarsening – upward” character typical of prograded barrier island marine sandstones (Cant, 1992). However, contradictions to that interpretation are as follows: (1) Except for the presence of scattered granule-size white and dark gray chert pebbles, a few centimeters below the top of the reservoir sandstone, observed in the Midwestern Gas Alexander 10-23-56-1 W5M core, detailed examination of cores from the two wells studied did not indicate any discernible increase in grain size from the bottom to the top of the reservoir sandstone. (2) The SP response of the reservoir sandstone at several wells, including the electric log designated by the letter “L” in Figure 1a and shown in Figure 4, does not show a distinctly “coarsening-upward” feature. According to Williams and Stelck (1975), in late early Albian time, an embayment of the Boreal ocean (Clearwater sea), characterized by the Subarcthoplites ammonite fauna, penetrated southeastward into Alberta and Saskatchewan to the latitude of Calgary. McLean and Wall (1981) show early arms of the Boreal sea as estuaries extending southeastward along the Spirit River and Edmonton channels of Alberta during deposition of Ostracode zone sediments. These boreal seaways were a precursor of the southward widespread marine flooding by the Moosebar-Clearwater sea (Figures 1b and 5).
Karvonen(1989) described and mapped an
Ostracode zone estuarine facies, (similar to facies within the Gironde
estuary on the Atlantic coast of France), in east central Alberta. The
evidence for the estuarine facies interpretation include sand-shale
tidal bundles and elements of both the Cruziana and Skolithus
ichnofacies considered by Karvonen to be indicative of brackish water
environments. Following McLean and Wall, (1981), Karvonen interprets
that an arm of the Boreal sea extended south and southeastward along the
Edmonton channel (and tributary channels) to a Based mainly on their widespread lateral extent, their relatively uniform tabular shape and excellent sorting and reservoir quality, the Alexander and Big Lake Gas Field reservoirs are interpreted as marine sheet sandstones. The present authors interpret that at the beginning of Ostracode zone deposition, the shoreline of the Boreal sea within the Edmonton channel was located at the present northwestern limit of the city of Edmonton. At this location, distribution of river mouth, or more likely estuarine mouth, sands by wave induced currents formed barrier islands. Under stable or falling sea level, it is suggested that the barrier islands may have prograded westward to form sheet sandstones as shown in Figure 6. Natural gas was trapped at the updip limit of the reservoir sandstones. The equivalent lower Ostracode zone dark brown to black argillaceous limestone at Campbell-Namao Field is considered to be a widespread lake or brackish water lagoonal bay facies. Karvonen and Pemberton (1997) also interpret progradation of Ostracode zone barrier islands (similar to those shown in Figure 6) in the Jenner-Suffield area, southeastern Alberta. During deposition of middle Ostracode zone strata, it is interpreted that a rise in sea level caused the Boreal sea to advance south and southeastward along the Edmonton and tributary channels to the Bellshill Lake area of Alberta. With the rise in sea level, sands were trapped in the Bellshill Lake estuary mapped by Karvonen (1989) and only clay and organic matter were deposited in the marine Edmonton channel near Edmonton. These clay and organic matter sediments buried the lower Ostracode zone sandstones at Alexander and Big Lake Fields (Figures 1a and 5).
The Ellerslie Member of the Mannville Group (Hunt 1950) consists primarily of well-rounded fine- to very fine-grained (Wentworth scale) quartz sandstones and dark gray shales containing coaly plant fragments. In the Edmonton area, the Ellerslie Member lies on the eroded surface of the Devonian Wabamun Formation. The unconformity is commonly marked by light green waxy-appearing claystone containing siderite spherulites and weathered chert fragments. Locally, thin quartz sandstones are interbedded within the claystone. These lithologies are commonly referred to as the Detrital zone (Deville Member) and are interpreted to represent an ancient soil horizon (Williams, 1963). The eroded surface of the Wabamun Formation (consisting mainly of limestone and very finely crystalline dolomite) exhibits considerable topographic relief. The Ellerslie Member is much thicker in valleys on the erosion surface and is thinner overlying ancient hills. The Ellerslie Member thus ranges in thickness from zero to more than 90 metres (300 feet). On the basis of Ellerslie thickness information obtained from boreholes, Williams (1963) mapped a drainage pattern of trunk rivers and tributaries that had eroded into gently southwesterly-dipping Devonian and Mississippian strata. The drainage pattern indicates that the trunk rivers flowed north to northwest. The Campbell-Namao Field is located near the axis of a main Ellerslie trunk river valley, named by Williams (1963) as the Edmonton channel (Figure 5). In the lower part of the Edmonton channel, the Ellerslie sandstones probably represent braided river deposits similar to present-day braided river deposits along the Niobrara River, Nebraska, including associated levee, crevasse splay and shallow lake deposits described by Ethridge et al. (1999). However in the Edmonton area, during deposition of the uppermost part of the Ellerslie Member, aggradation of sediments had filled the original valley and leveled the surface topography, forming a widespread flood plain. As the rivers continued to flow they excavated channels into pre-existing sediments, meandered, and avulsed across the terrain. As shown in Figure 7, towards the end of Ellerslie deposition, minor hills and valleys on the eroded surface of the Wabamun Formation had little or no discernible influence on the path selected by the river in its journey to the sea. In upper Ellerslie interfluve areas near the city of Edmonton, (Figure 8), the upper part of the Ellerslie Member can be readily correlated on electric logs and consists of two sheet-like quartz sandstones, each about 5 metres thick separated by an electrically resistive marker bed (2 metres thick) (Figure 9). For mapping purposes, these two sandstones are hereby referred to as Peavey and Acheson sandstones. Because of their relatively uniform thickness and widespread lateral extent, the two sandstones are interpreted to have formed by seaward progradation of barrier islands similar to formation of the lower Ostracode zone sandstone at Alexander and Big Lake gas fields. Like many shoreface marine sandstones, both the Peavey and Acheson sandstones contain stratigraphically trapped gas and oil accumulations (Figures 1a, 9, and 10). At Saddle Lake, Alberta, (120 km northeast of Edmonton), an interpreted rapid and substantial rise in sea level at the beginning of Joli Fou time, resulted in preservation of levee and crevasse splay deposits associated with an uppermost Mannville (Colony) meander belt (Edie and Andrichuk, 2003). However, in the Edmonton area, at the beginning of Peavey Sandstone deposition, a marine transgression (forming a ravinement surface as defined by Nummedal et al., 1987) is interpreted to have destroyed levee and crevasse splay deposits leaving an electrically resistive lag (marker bed) in interfluve areas. A wireline core from this marker bed at Pacific British Dominion Woodbend 4-36-51-26 W4M in the interval 4176-79 ft. consists of calcite cemented very fine-grained quartz sandstone containing scattered gastropod shells and shell fragments. A 15-cm-thick dark gray shale bed is present at both the top and bottom of the calcite cemented sandstone. Hayes (1989) has documented marine barrier island retreat caused by marine transgression along a section of the South Carolina Atlantic Coast. This local marine transgression has resulted from a reduction in sediment supply due to construction of dams on the Santee River. Hayes recognized that the marine transgression, which recently cut a submarine terrace across the upper portion of a barrier island, is now eroding into back-barrier island marsh sediments containing tidal creeks and oyster reefs. Thus, Hayes has direct evidence that this local marine transgression will result in a shelly transgressive lag deposit similar to that in the aforementioned 4-36-51-26W4 borehole formed at the toe of the retreating shoreface. According to Hayes, continued transgression may result in the loss of the top 3 to 4 metres of the stratigraphic record.
Figures 11-20
Meander Belt Facies
At Campbell-Namao Field, detailed
microscopic examination of well bore cuttings by the authors showed that
Cores from four wells (Lsd 4 Sec. 6 –
T55 R24W4, and Lsd 1 Sec. 1, Lsd 2 Sec. 1 and Lsd 3 Sec. 1 in T55 R25W4)
taken from the middle to lower parts of
An electric log trace of a resistive
gas- and oil-bearing interpreted
As shown in Figures 13,
14 and 20,
individual hydrocarbon-bearing
As shown in Figure 14, a number of
boreholes intersected water-bearing
In the absence of cores to identify
basal lag deposits, the base of Typically, the electric log response of coastal marine sandstones, including those of barrier island origin, reflects the coarsening-upward texture of the sandstone (Cant, 1992). For example, electric logs of the Cretaceous marine middle Viking reservoir sandstone at Joarcam oil and gas field, central Alberta, clearly show this coarsening-upward feature (Edie, 1955).
In contrast, as illustrated by Coleman
and Prior (1982), valley fill sandstones, characterized by fining-upward
response on electric logs may represent either linear braided channel
deposits or highly meandering river An excellent example of a linear channel within the Mannville Group, characterized by four fining upward cycles is documented by Matheson (1988), who made a detailed study of a heavy oil reservoir sandstone at Fort Kent, Alberta (190 km northeast of Edmonton). The cycles consist of intraformational conglomerates composed of gray shale intraclasts in a sandstone matrix and fine to very fine sandstones grading upward to silty shale. The depth of the incision was approximately 20 metres.
At Campbell-Namao Field, the lack of
multiple fining-upward cycles within the roughly 20-metre-thick
lenticular sandstones indicates that the sandstone bodies are not
stacked braided river channel deposits but instead are
An examination of the SP curves of
interpreted relatively clean
Collinson (1978) points out that with
respect to lateral extents and thicknesses of alluvial sand bodies in a
river meander belt, an empirical relationship exists between bankfull
depth of the channel (presumably equivalent to
Flach and Mossop (1985) in detailed
outcrop studies along the Steepbank River, near Fort McMurray, Alberta,
showed that oil-bearing
In describing the McMurray Formation
outcrops along the Steepbank River, Flach and Mossop (1985) and Wightman
and Pemberton (1997) cite trace fossil evidence for estuarine origin.
However, Flach and Mossop (1985)
At Campbell-Namao Field, permeable
fining-upward sandstone with interbedded shale beds of sufficient
thickness to be recorded on the SP curve are readily recognized on
electric logs and are defined as shaly
Smith (1987) in detailed field studies using vibracores and trenches,
showed that inclined interbedded sand and shale beds (inclined
heterolithic stratification) characterize low energy
Wood (1989), in detailed mapping of
almost continuous outcrops of the Upper Cretaceous Judith River
Formation in the badlands of the Red Deer River Valley, Alberta,
demonstrated that clean
As interpreted by Wood (1989), the IHS beds of the Judith River
Formation formed during low-energy conditions, caused by reduced local
gradient in late stages of formation of a meander loop, prior to meander
cut-off (Figure 17). In this situation, the gradient within the meander
loop decreases to almost zero as the meander loop continues to lengthen
with the same overall vertical drop. This local decrease in gradient
results in reduced current velocity and apparent increased sedimentation
of suspended clays and silts on the downstream portion of the
Shale-Filled Channels or Oxbows In the Campbell-Namao field area, 14 boreholes intersected shale-filled channels or oxbows (Figures 14 and 18) as follows:
Several cores from early-drilled boreholes in the Campbell-Namao Field show that shale-filled channels consist mainly of gray-black fissile shale containing coaly plant fragments and locally contain 10 to 40% lenses and thin beds of siltstone and very fine sandstone that exhibit penecontemporaneous slump structures with dips from near horizontal to vertical (Figure 11). Dark brown sideritic nodules or lenses up to 1 cm thick are also common. Compared with the low resistivity of Mannville pure shales, shale-filled channels or oxbows typically exhibit higher resistivity on electric logs (Figures 13, 18, and 20). Presumably, the increased resistivity is due to the presence of siltstone and very fine sandstone lenses and the siderite nodules. Of the 14 shale-filled channels intersected in boreholes in the Campbell-Namao field area, 11 appear to represent the central portions of channels and three thinner shale intersections appear to have been drilled on a channel edge. The thickness of the aforementioned centrally located shale-filled channels varies from 14.6 to 23.5 metres (48 to 77 feet) and the average thickness is 17.8 metres (58.4 feet). The variation in thickness of shale-filled channels in several boreholes in Campbell-Namao Field is shown in Figures 13, 19, and 20. The variation in thickness probably is caused by the following factors:
As shown in Figures 13, 19, and 20, because of differential compaction, the top of the Ellerslie Member is invariably structurally low where a borehole intersected a shale-filled channel.
Figures 21-27
Meander Belt Sedimentation
Based on electric log character of readily correlatable interfluve
facies (Figures 4, 9, and
10) and electric log character of meander belt facies ( Within the productive portions of the meander belt, it became obvious that the 20-metre-thick reservoir sandstone was highly compartmentalized. The compartments were characterized by marked differences in the thickness of the oil column and marked differences in the subsea elevation of gas-oil and oil-water contacts. Examples of the differences in oil column thickness and differences in the elevation of gas-oil and oil-water contacts are shown on sections G-H and X-X' across and within the meander belt (Figures 14 and 20) and on section J-K along the meander belt (Figures 14 and 19). During development drilling of the Campbell-Namao Field, seismic techniques had not yet been developed to trace the precise location of shale-filled channels or the extent of individual hydrocarbon compartments. Thus, in an attempt to map the extent of individual compartments, groups of wells with essentially the same oil column thickness and the same subsea elevation of gas-oil and oil-water contacts were circumscribed by a shale filled channel. Although this mapping was aided by incorporating the location of 14 boreholes that intersected shale-filled channels, paucity of well control in some parts of the field permits only the approximate shape and extent of some compartments to be outlined.
In plan view (Figure 14), the less
extensive In the southern part of Figure 14, the meander belt is 3.2 km (two miles) wide. Northward, the meander belt abruptly widens to 5.6-8.0 km (3½ to 5 miles), and that widening is interpreted to be due to avulsion and the establishment of a slightly younger sub-parallel meander belt, as shown in Figure 21. As on modern flood plains, Mannville meandering rivers probably were characterized by periodic channel switching. As a river meanders, natural levees and crevasse splays form during seasonal flooding and overbank flow (Allen, 1965). The levees gradually build up by vertical accretion above the level of the back-swamp or flood plain until such time as conditions become unstable and the river breaks out and excavates a new channel to the sea (avulsion) (Figures 8 and 22). As pointed out by Wood (1989), the initial channel in this process of avulsion is relatively straight. Also, in the case of large rivers, the excavated channel may be very deep. For example, the meandering portion of the Mississippi River at Baton Rouge, Louisiana, has excavated a channel 35 metres deep; i.e., from a surface elevation of 10 metres above sea level (top of the levee) to a depth of 25 metres below sea level (Farrell, 1987).
As depicted in Figure 22, as a newly
avulsed river begins to meander, it erodes the cutbank in previously
deposited sediments. Also, if the amount of sediment in the river system
exceeds its carrying capacity, a sandy
Internal Meander Belt EntrapmentAn examination of cross sections (Figures 19 and 20) and structure contours on top of the Ellerslie Member (Figure 23) show that although there is considerable structural warping of the Ellerslie Member, the main element in hydrocarbon entrapment within the meander belt is stratigraphic control. Structural warping definitely enhances or decreases the pay thickness at individual wells but in general is not a controlling factor in entrapment. Masters (1984) points out that the McMurray oil sands represent an immense anticlinal closure, 150 miles long by 70 miles wide, caused by updip eastward dissolution of thick Middle Devonian salt. He postulates that: (1) the oil sands represent an enormous light gravity oil accumulation that was later biodegraded to its present viscous state, and (2) that the source of the oil was Lower Cretaceous shales and older Mesozoic shales of the deep Alberta basin.
In contrast, Stanton (2003, 2004) in a
scholarly geochemical treatise concludes that in terms of sheer
magnitude, there is insufficient volume of Lower Cretaceous and Jurassic
black shale source beds in western Alberta to account for the enormous
quantities of heavy oil and bitumen in eastern Alberta. On the other
hand, he notes that in the deep basin, foothills and mountains, vast
quantities of coal occur within Lower Cretaceous - Jurassic interval. He
therefore postulates that most of the aforementioned heavy oil and
bitumen represent light gravity oil formed during bituminization of vast
quantities of coal source beds, with only a minor portion being derived
from the interbedded black shale. Stanton believes that the original
light gravity oil followed permeable zones along the pre-Cretaceous
unconformity and was later biodegraded. In any case, if originally vast
quantities of light gravity oil and gas were squeezed out of deep basin
Lower Cretaceous and Jurassic source beds, it follows that all Lower
Cretaceous stratigraphic and structural traps along the migration path
were filled to spill
Because the gas caps at Campbell-Namao
Field are invariably oil stained, it is interpreted that light gravity
oil first entered all the traps and filled them to spill
External Meander Belt EntrapmentThe curved shape of the meander belt shown in Figure 14 is also a controlling factor in truncation type stratigraphic traps illustrated in Figure 25. Because of the curvature of the downdip (southwestern) edge of the meander belt, deeply entrenched shale-filled channels are interpreted to have caused both updip and lateral stratigraphic entrapment within two sheet sandstones (the Acheson Sandstone and the next underlying sandstone) of the interfluve facies. A stratigraphic trap within the Peavey Sandstone, similar to that shown in Figure 9, overlies the two truncation type traps (Figure 25).
As shown in Figures 23 and
25, the oil
columns in the Peavey and Acheson sandstones extends 4 km (2 ½ miles)
down-dip from their structurally highest The closed low structure on the eroded top of the Wabamun Formation, marked by the -470 and -480m subsea contours near the center of Figure 7, is interpreted to be a karst structure caused by collapse of the roof of a cave within the Wabamun Formation after the Ellerslie Member was deposited. For example, contours on top of the Ellerslie Member (Figure 23) reveal a distinct syncline separating the two Peavey Sandstone gas-caps and that syncline coincides with the interpreted collapse structure on the eroded top of the Wabamun Formation. In central Alberta, where the Wabamun Formation is truncated by pre-Cretaceous erosion, there is local evidence of karsting or open caverns at or below the eroded top of the Wabamun. For example, in Wabamun core studies associated with his paper, Andrichuk (1960) described dolomite solution breccias with waxy green claystone matrix, tens of metres thick, occurring at the eroded top of the Wabamun at Union Storvick 13-28-46-17 W4M. Also, Glaister (pers. comm., 2003) states that in 1954, at Imperial Rosalind 8-9-44-17 W4M, after drilling a short distance into the Wabamun with no problems, the bit suddenly dropped about 7 metres and circulation was lost for over 2 months before the well was abandoned. Drilling then commenced immediately on the adjoining Lsd 9 and total depth at that location was reached in the Beaverhill Lake Formation without any Wabamun lost circulation problems.
Structural EntrapmentIn upper Ellerslie interfluve areas near Edmonton, numerous anticlinal gas and oil accumulations occur in the upper part of the Ellerslie Member. In the thin sandstone beds that characterize the interfluve areas, only slight structural closure is required to trap hydrocarbons, and in some cases, pay zones are stacked. Drillstem tests of those thin sandstone beds commonly yielded up to 28.2 x 103 m3 (1 million cubic feet) of gas per day with very little pressure drop in a one hour test. However, due to the typically small areal extent of the traps, such gas wells often water-out after only minor production (Figure 26). As illustrated in Figure 27, minor upper Ellerslie Member anticlinal structures can occur due to:
As shown in
Figure 19, a 4-metre
(13-feet)-thick upper Ellerslie gas accumulation at the 14-6 well is
interpreted as due to local structural warping of a mainly water-bearing
Conclusions
In central Alberta, upper Ellerslie
meander belts are mapped from electric logs with relatively sparse well
control. In exploratory drilling along these meander belts, hydrocarbon
reserves similar in size to those in productive
The exploration procedure outlined
herein applies to meander belts of various ages world-wide provided that
(1) the
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The authors thank Oscar A. Erdman, R. Perry Glaister, Grant D. Mossop, and Gordon D. Williams for reading the manuscript and offering suggestions for improvement. Editor Tim de Freitas and Associate Editor James M. Wood, Canadian Society of Petroleum Geologists, also offered many helpful suggestions for improvement of the text and figures. The writers are also grateful to Regina Shedd at the Gallagher Library, University of Calgary, for assistance in obtaining important geological references, and to David G. Sargent, for computer drafting of the figures. |
