Basement Controls on Red River Sedimentation and Hydrocarbon Production in Southeastern

L.K. Kreis and D.M Kent I

Kreis, L.K. and Kent, D.M. (2000): Basement controls on Red River sedimentation and hydrocarbon production in southeastern Saskatchewan; in Summary of Investigations 2000, Volume I , Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 2000-4.1.

1. Introduction 2. Regional Basement Features Discovery of significant oil reserves in Red River strata The origin and nature of the are in the Berkley et al. 4-2-7-11 W2 well in unclear and their discussion is beyond the scope of this December 1995, together with Saskatchewan paper (for further infonnation see Stewart, 1972; government incentives such as reversion of deep rights Dickinson, 1976; Gerhard et al. , 1982; Kent, 1987; to the Crown in I 998 and reduced royalties for deep Crowley et al., I 985; Fowler and Nisbet, 1985; Green exploration and development wells, set the stage for et al., I 985a, I 985b; Green et al., 1986; Quinlan, 1987; recent hydrocarbon exploration activity targeting Red Gerhard et al., 199 I; Sims et al., 1991 ; Burwash et al., River rocks and, to a lesser extent, the Winnipeg 1993; Nelson el al., 1993; Kent and Christopher, 1994; Formation. Between December 1995 and December Baird et al., 1995; and Gibson, I 995). 1999, over 280 wells have been licensed to explore the Red River in southeastern Saskatchewan. More than Three major basement provinces are recognized from half of these were licensed to drill to the Precambrian; regional magnetic data in the Williston Basin area they have provided valuable new information about the (Green et al., 1985a, l 985b; Baird et al., 1995; Gibson, Precambrian basement surface, basement structure and 1995; and Kreis et al., 2000). Archean (>2.5 billion lithology, and relationship between basement and years) rocks of the Wyoming Province in the west and overlying strata. Oil exploration companies have taken the Superior Province in the east are separated by an cores in most of these wells, greatly contributing to our intervening collage of Proterozoic rocks belonging to understanding of deep formati ons. the Trans-Hudson Orogen (1.8 to 1.9 billion years) (Figure 2). The Trans-Hudson Orogen is considered by Prior to the Midale discovery, Red River production Lewry and Collerson ( 1990) to be a major component was restricted to l 6 wells widely distributed in the of the Early Proterozoic Pan-American orogenic Minton, Hummingbird, , Beaubier, , system, extending from South Dakota, across Hudson Bromhead, and Weir Hill areas near the American Bay, Greenland, and Labrador. Results from the border in southeastern Saskatchewan (Figure 1). Since COCORP deep reflection seismic transect in then, producing reservoirs have been discovered up to northeastern Montana and northern North Dakota 7 5 km northward into the Chapleau Lake area. suggest that the Trans-Hudson Orogen is probably Numerous seismic surveys covering large areas to the cored by an Archean crustal fragment that was caught north and west of these producing areas have been run up in the collision of the two Archean paleocontinents in recent years, holding the promise of further drilling (Baird et al., 1995). and more discoveries. Recently, a deep well test has been li censed to drill to the Precambrian basement in Mappable features that are spatially related to the Township 27 and Range 18 west of the second boundaries of the basement provinces (Figure 2) and meridian, some 125 km north of Chapleau Lake. In th e that are defined by thickness anomalies in various 38 years following the first discovery in 1957 until the Phanerozoic fo rmations or by geophysical mapping Midale discovery, oil production from Red River include the Birdtail-Waskada axis, a well known north­ reservoirs totaled just over 226 000 m3 from 16 wells. south lineament lying immediately east of th e In fewer than fo ur years between the Midale discovery Saskatchewan-Manitoba border. Characterized by and mid-September 1999, more than one million cubic numerous structural and stratigraphic irregularities metres of oil have been produced from 115 new wells. (McCabe, 1967; Dietrich and Magnusson, 1998), it directly overli es the boundary between the Trans­ This paper focuses on stratigraphic evidence for Hudson (Churchill) and Superior provinces. Andrichuk basement controls on Red River sedimentation and ( 1959), Kent ( 1960), Christopher ( 1961), Kendall hydrocarbon production in southeastern Saskatchewan, ( 1976), and Kreis ( 199 1) document thinning of various an area on the northeastern margin of the Williston Phanerozoic units in a north-south zone parallel to the Basin (Figures I and 2). It also d iscusses spatial Saskatchewan-Manitoba border in southeastern relati onshi ps and orientations of basement features and Saskatchewan. This area coincides with the Nelson lineaments.

' D.M Kent Consulting Geolog ist Ltd .. 86 Mctcallc Road. Regina. SK S4V 01 18.

Saskatchewan Geological S urvey 21 -=~~~~=~~,--~---.:;:::--~1J------,:----,,:,------23 51°00' "' 22 + '21 ._- ---~-:~i ::

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::::,~' ) en I /

0, 300km i 0 200Mi 11 WILLISTON BASIN OUTLINE IJU 1.4.EDGE-PRAIRIE EVAPORITE ANTICLINES ····•··•· EDGE-PALEOZOIC EDGE OF ARCHEAN CRATONS 11111111111111 NACP CONDUCTOR ZONE HEAT FLOW ANOMALIES BIRDTAIL-WASKADA AXIS , • ··,...... MISSOURI COTEAU STUDY AREA D 1,,,:._ ._ ,· -::b/ / / __ i·;'.I/_/ NELSON RIVER GRAVITY TREND .,,.,. LINEAMENTS .,,.,... 1.) BROCKTON- FROID - FROMBERG FAULT ZONE 2.) COLORADO - WYOMING FAULT ZONE

Figure 2 - Map showing major Precambrian basement features and subsurface and suiface lineaments within and conterminous with the study area (modified from Kent, 1987; Majorowicz et al., 1988; and Baird et al., 1995).

Saskatchewan Geological Survey 23 River Gravity Trend (Macdonald and Broughton, nomenclature) over the interval from 2315 to 2327. 7 m 1980) (Figure 2). which includes the lower Coronach, Lake Alma Anhydrite and "C" Laminated. The upper 7.1 m of the Two wells, Imperial Lightning Creek 16-7 -6-32 WI core have a typical Herald succession of burrow­ and Cherokee et al. Workman 2-34- l-32W1, in mottled overlying a thin laminated dolostone southeastern Saskatchewan are located in a north-south all belonging to the Coronach. They rest upon a 3 m zone parallel to the nearby Birdtail-Waskada axis. thick evaporitic interval consisting of 1.6 rn and 0.8 m They show evidence of faulting which could be of interlaminated dolostone and anhydrite separated by attributed to basement movements within this major 0.6 m of laminated dolomicrite and oolitic-intraclastic paleotectonic zone (Figures 1 and 2). The evidence dolo-wackestone. The evaporitic interval is in contact includes Kendall's (] 976) observation that the Red with typical "C" Laminated rocks. A repeated sequence River interval is anomalously thick (more than 60 m of Lake Alma Anhydrite forms the next 5 .6 m of core. greater than normal) in the Lightning Creek well. He In addition, the interval from 2325 to 2325.7 m attributes this thickening to apparent repeated sections contains deformed dolomicrite with a dip of 40° to 45°. in geophysical well logs as well as repetition of Repetition of strata in both the Lightning Creek and Deadwood lithologies in well cuttings at a stratigraphic Workman wells suggests reverse or thrust faulting may level where Red River rocks would normally occur. He have occurred in these intervals. The Interaction also comments on the unusual thickness of dolomitized Renata Workman 3-27-l-32Wl well shows a rock in this well. This feature contrasts with the pronounced thinning of Red River strata over a partially dolomitized Yeoman sections in nearby wells basement high (Figure 4). The anomalous thinning and and indicates an unusual diagenetic history, possibly the faulting in this well suggest syn- and post­ related to faulting. The Workman well is cored in the depositional reactivation of the basement. Bighorn Group (see Figure 3 for stratigraphic The coincidence of the North American Central Plains electrical conductivity anomaly (NACP) with the Trans-Hudson Orogen S.E. SASKATCHEWAN NORTH DAKOTA implies a Precambrian basement KENDALL (1976) KOHM AND LOUDEN (1978) structural control to the feature (Figure 2). The presence ofhigh­ STONEWALL FM. STONEWALL FM. grade metamorphic rocks in drill core samples and of a narrower >- GUNTON MBR. zz~ . width of the Trans-Hudson zz. 01-~ segment in North and South I-~ LL STONY MOUNTAIN SHALE Dakota relative to the exposed 01-~ GUNN MBR. Cl) !-~LL segment in the Cf) HARTAVEN MBR. suggest that compression during .. A.. z "A" ANHYDRITE MBR. '""> collision was greater in the oO REDVERS UNIT Williston Basin area (Baird et al., _JI- CORONArH ANHY. > "B" ANHYDRITE MBR. 1995). Majorowicz et al. ( 1986, 'B" LAMINATED MBR. 1988) and Osadetz et al. ( 1998) ~~ CORONACH MBR. 'B' BURROWED MBR discuss a heat flow anomaly that w 0:: -,. IQ LAKE ALMA ANHY. "C" ANHYDRITE MBR. is situated near , LL LAKE ALMA MBR. "C" LAMINATED MBR. immediately east of the NACP z along I 03°W (Figure 2). It 0:: 0 w j::: juxtaposes an electrical <( conductivity anomaly found from > ~ 0:: a magnetotelluric (MT) study 0:: 0 0 u.. reported by Jones and Savage w 0:: ( 1986). Both the heat flow and 0:: UJ YEOMAN FORMATION > "C" BURROWED MBR. electrical MT conductivity 0:: anomalies coincide with a 0 UJ significant Williston Basin 0:: feature, the Nesson Anticline (Majorowicz et al., 1988), which has been active throughout Phanerozoic history (Gerhard et al., 1982).

Features that appear to be WINNIPEG FORMATION WINNIPEG SHALE spatially related to the interpreted northeastern margin of the Wyoming Province in Figure 3 - Correlation chart showing stratigraphic nomenclature of Red River southeastern Saskatchewan (Yeoman and Hemld) am/ adjacent strata in Saskatchewan and North Dakota. include some predominantly

24 Summary of Investigations 2000, Volume l SHEU. SOllTH OXBOW V1STAGLEN EWEN SlllliWO~ INTERACTIONRENATA PLACID el al WORKMAN 13-24-2-3W2M 16-23-2-3W2M 16-1 9-1-32W1M WORKMAN 2-7-1-31W1M - K.B.: 570.6m KB: 557 3m K.8 .. 518.Bm 3-27-1-32W1M K.B.: 504.4 K.B.: 502.Sm 2: -¢-19.4km-¢- 22.2km 4.4km 7.2km zct: B -¢- -¢- B' 0 > w w • E 0 OATIJM: TO!' OF ASH ERN 2400 AS HERN 2100 23- 2100 - 2200 z -<.:: INTERLAKE r:= 2~0- O' 2200 ::::, --' 2400 --~- 2200 en 23~

2600 ... STONEWALL 2300 - STONY MOUNTAIN 2SOO 2400 O' HERALD z w 2700 ct: 2400 lJ > > a'.'. 2600 2400 0 c, YEOMAN 2500--~--L- - 0 w a:: a'.'. - ·-· ~ 0 " ------I ,m - I 2100 ' + WINNIPEG + ?500 I I 2600 + ... + + + + L L + 2900 :,roi~ ~ DEADWOOD + - t I I ---- ! 1BOO - + ... - + - T + - + ... + ... + ... '·' I I I I I I I - I I· + + ' + + + ' + I + + + + - + + ...... + !- !- T - + + PRECAMBRIAN r+- lt-1000 + ------L I I L + I· + + + + + ... + + + + + + + + Figure 4 - Cross-section B·B' (see Figure 1) showing Precambrian puleotopographic high in the Interaction Renata Workman 3-27-1-32Wl well. Note thinning ofthe Red River section in thi.~ well (modified from Haid/ et al., in press). northwest-trending multistage salt-solution structures Stauffer and Gendzwill, 1987; Brown and Brown, and major seismic positive clements (Kent, 1973). The 1987; Penner and Mollard, 1991; Misra eta/., 1991; northeast margin of the present-day salt dissolution Gibson, 1995). Some of these lineaments are edge of the Prairie Evaporite is subparallel to the recognized by surface structure, stratigraphic contacts, northeastern edge of the Wyoming Province (Figure 2), and geomorphic anomalies from air photos (Thomas, as are surficial topographic lineaments formed by 1974), others by integrating a variety of data sets from Wascana Creek, Creek and Souris River geological, geophysical, geochemical, and waterways and the northeastern edge of the Missouri hydrogeological sources (Brown and Brown, 1987; Coteau (Figure 5). The Elbow-Weybum trend (Figures Mollard, 1988; Penner and Mollard, 199 I). The 2 and 5) of Paleozoic age is also oriented northwest­ dominant lineament trends in southern Saskatchewan southeast (Christopher, 1980). are about N50°E, N50°W, N35°W, and N35°E (Penner and Mollard, 1991) (Figure 6). Wascana Creek, Moose Jaw Creek, and Souris River each have a U-turn which reverses their flow direction Misra et al. (1991) employed remotely sensed Landsat (Figure 5). These turns are located in or near a MSS, TM, and Seasat satellite radar images to derive northeast- trending area that approximately aligns with lineament maps. They found no obvious relationship the northeastern edge of Prairie Evaporite solution. between patterns found on regional magnetic maps and Also, Moose Mountain Creek and Long Creek brittle fractures in Phanerozoic strata. They also commence close to this area, in which the Minton, mapped a ca. I 00 km wide northwest-trending linear Ceylon, , Tyvan, and Chapleau Lake Red River feature, the Central Fault Zone (CFZ), extending from producing areas are situated. These and other Red northern Alberta to the U.S. border southeast of River producing areas, and their correlation with Regina, and apparently defining the northeastern regional lineaments interpreted from airphoto and margin of the Wyoming Province in the basement of satellite images, along with subsurface geological and southeastern Saskatchewan. geophysical data sets, have been recognized by Penner (in Mollard, 1999, Figure 31 a). Gerhard et al. ( 1991) related major faults and fault folds in the Williston Basin to a hypothetical Numerous authors have recognized Precambrian Proterozoic wrench-fault system dominated by two basement structural controls on sedimentation within major northeast-trending left-lateral, strike-slip fault the Williston Basin (Kent, 1973, 1974, 1987; Potter zones (the Brockton-Froid-Fromberg and Wyoming­ and St. Onge, 1991; Kissling, 1997). Some have Colorado) (Figure 2). They suggested that: a) little described a predominance of lineaments with evidence exists for Phanerozoic left-lateral motion northeasterly and northwesterly strikes which they along the two zones and b) the dominant movement in attribute to regional stresses in Precambrian basement the Phanerozoic has been vertical. rocks (Thomas, 1974; Bell and Babcock, 1986;

Saskatchewan Geological Survey 25 ...., ,~ ' ,_,..-----...-- I _i._:P:,:-l--1_ ---1,23 51"00' I , , \--r-- !\ -f. I 1 , L -1~ °' l__±_i__ : 22 -r i -~~ · +ic;ci +j: ~ 1 ·t19 ...... ,,. ..--. .. c.. :E en c: ~ I-

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~ § ~ -~ ., ' -r;A~. 49°00 2 1 34 33 32 31 30 ~ 30 29 28 27 11 10 9 B ·-5 4 ·3 :::, 106'00' 102°00· -­ei 103°00' ~ Range W2 W1 ~· NORTH DAKOTA ~ c;· + Well Locations ....,~ ::::, Areas of Red River ::::, + Lighting Creek Structure _::::, Production ~ Edge of Prairie Evaporite & Workman Structure ~ Figure 5 -*Missouri Coteau, Elbow- trend, and water drainage show a northwest-l·outheust orientation. U-bemls cuu~·ing the Wuscana Creek, ,Hoose Jaw Creek, 3 and Souris River to reverse their flow directions are located in or 11ear u 11ortheast-trendi11g area indicated by dark grey shading. Also, Moose /l,fou11tai11 and Long Creeks "' rise close to this area. 105° J 70 m as determined fr om th e Deadwood isopach I map. T he extent and configuration of this featur~ SASKATCHEWAN cannot current Iv be determined from mapping smce no other nearby w~ lls penetrate the Precambrian. A . Prince AlbeI rt seismic structure map at the level of the sub-Mesozoic Ll oydm,ns! er surface centred over this well (from Sawatzky in Holter, 1969) and recently processed gravity data in the vicinity define a feature about 5 km ~~ ~ sko1oon across (Miles et al. , 2000 ). _JI Y . In th e past few years, exploration compa~ies have

Sw, !1 Current 1' oREGINA (Hai d! et al. , in press). They ther~foi:e atte!11pt to dnll 1 I 1 Rocorwille over basement highs only, resultmg m a biased . I Moose Jow ~ _ .. ·-/-;; · 50• distribution of well control. Nevertheless, we believe - G~ -- ·-~ ·· wey\vr~~\ that suffic ient control exists to outline some basement 1 linear features that are I ikely to be fault controlled. We J_ • Shounovon Este van, l envisage that the relief along these Precambrian ------paleotopographic lineaments ranges (rom a fe~ tens of Figure 6 - Map ofsouth ern Saskatchewan -~ho':ing double metres to at least 170 m and is essentially continuous suborthogonul fracture lineament .fystems, uultcuted by over distances up to ca. 70 km (Figure 11 ). M ilkereit et heavy t/11rk lines.from eight study areas (from Mollartl, al. ( 1995) described Precambrian base~ ent features of 1988). similar dimensions in central Alberta, mterpreted from deep seismic reflection data. Gough and Bell ( 198 1) , Bell and Babcock~ 1986), and Bell et al. ( 1994) believe that stresses causmg Pre-Deadwood differential eros ion may have played breakouts in well bores across western some role in creating the paleotopography on the orioinatc in the lithosphere. They determined that the Precambrian basement in southeastern Saskatchewan. ma~imum horizontal stress is oriented northeast­ However as most of the rock samples from both southwcst and speculated that this a_nisotropy in t~e Precamb;ian highs and lows e~amined in.th_is study stress regime is the result of drag e ffects as the m1d­ appear to be lithologicall y similar (grantllc m . American lithosphere is pushed northeastward by a composition), most of the basement paleotopography 1s rising mantle convection cell beneath western North interpreted to be the result of movement along fault America. zones that were active prior to, during, and after Deadwood sedimentation. 3. Local Basement Features A remarkable feature of the Deadwood isopach map in southeastern Saskatchewan is the northwest and A province-wide Lower Paleozoic mapping project northeast orientation of basement highs, defined by initiated by staff of the Petroleum Geology Branch of Deadwood isopach thins (Figure 12). This is strikingly Saskatchewan Energy and Mines is complete. . similar to the orthogonal pattern of surface and Structural and stratigraph ic information from this subsurface lineaments described previously (Figures 2, mapping shows a spatial relationship bet~een _ 5, and 6), implying that the basement highs are paleotopographic highs on the _Precambrian cryst~tlme g eneti cally re lated to the lineaments, perhaps b)'. a basement and structural and thickness anomalies m stress regime in the Precambrian basem~nt_th at 1s overlying Lower Paleozoic strata such as the periodically reactivated. The close prox1m.1ty of Deadwood and Red River formations (Figures 7 to 10). anomalously high Precambrian basement m the For example, the isopach map of the Dead~ood Amerada Crown SAD 13-12- l4-24W2 well with a Formation in southeastern Saskatchewan (Fig ure 7) reported s ite ofa magnitude 5 (Richter Sc~le). . clearly reflects areas of high relief on the Precambrian earthquake may be evidence of such react1vat10~ !n . basement surface (F igure 9). A ca. 70 km long recent times (Figures 7 and 13). Earthquake act1 v uy m northeast-trending zone of thin Deadwood joining the th is re"ion is thought to be related to movement along Midale, Froude, Hartaven, Corning, and Fillmore areas fa ults between blocks of rig id basement. MoI lard (Figure 7 ) forms the longest Precambrian ridge-like ( 1987) shows that th e di stribution of seism ici ty has feature discernible from current well contro l. These northwesterly, northeasterly. and northerly trends features are interpreted to be linear zones comprised of (Fi" ure 13). He also notes that th e southwestward small fau lt blocks in an en echelon arrangement. cxt~nsion of the basement high trend in Figure 12 Clastic sediments of the appear passes directl y be low an offset in the course ?f t~c to have onlappcd and infi lled areas around Souris Ri ver (Township 5, Range I 2 W:2) which 1s Precambrian basement highs. accompan icd by a drop in base level (Figure 14),. and sug,oests that these changes may be due to tecton1sm. The Amerada Crown SAD 13- 12- 14-24W2 well is Tl;;; basement high trend is parallel to th e Brockton- located over the highest known basement uplift, ca.

.'i'11sk 11tchn l'll11 ( il!oi"Kicol .Survey 27 "-' Oo 51°00'

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TC ~" i"' · :; ;;; 30 29 28 27 26 25 24 23 22 21 20 49°00' "'~ 106°00· 10 9 6 7 1 ~ 105°00· -~ Range W2 103°00' 102°00· g. W1 § Areas of Red River NORTH DAKOTA "' production + Lighting Creek Structure * Figure 7 - Deadwood isopach map (from Kreis, lOOOa). Contour interval is 20 m 4. Workman Structure (­ g~ I \ 1 Z\ I ) I 7 "'7 + I J 7 7 7\. :A'l 7 I 123 51·00· ~ 22 "' ::5 ::, ·~ 9- 13 a. ~ ~ ~ c:: ) 'C"' ~

30 is 2B 27 26 25 49°00' 10s·oo· 161 15 14 13 12 11 10 1Q4°00' Range W2 W1 MONTANA I NORTH DAKOTA

'" " Figure 8 - Red River isopach map (from Kreis and Haid/, 2000). Contour interval is 5 ,n ..... :::::, i

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? ·~I ~ -­ 49•00· ~ "~ 6 5 4 21 20 19 18 17 ¥ 27 26 25 24 23 22 W1 ~ 1os·oo· ""' Range W2 NORTH DAKOTA '"':::::, MONTANA ~ _:::::,

f,,. Fig ure 9 - Precambrian structure map (from Kreis ef al. , 2000). Contour interval is 30 m C/'

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49°00' 11 10 Range W2 1()_4°00' MONTANA I NORTH DAKOTA W1 .._...... Figure IO - Red River structure map (from Kreis a11d Haid/, 2000). Contour interval is 30 m. ..,_, ""'

A -¢- e e e A' ;:- tilnJ,,:~ &;,,r~ a;:, t'arL..-i,'V FC.i'1 :::.:tr:; i'. ;-:: t":1.rt~t!t' r·ihnk ColnrJ.:: 'f'i -9:_ •.. ~A- ~,m· · K.B 612, KB .. 624.2 ~. .B .. 625.9 K.B 659 .5 KB .. 669.5 E w ·0 ·..: .;.. 1 \',?,i il\·~· t::~ '1-121:' · ~-'T-l~: .fW2M :i.+1.2-1·:, a : 4·2t,· 12·El/2M (, ., ~ !":1,:,; . ) ~ i.._,, STCl.i ,,. t.1:J~,-AlfJ 1, ~ ~ ~ { (F t' ) t ' HEF

'~ ~ ~ <: "' Figure 11 - Cross-section A-A' along axis ofnortheast-trending positive paleotopographic relief on Precambrian surface. Note that the 10-14-9-11 W2 well is slightly of/­ f"' trend (see Figure 1) and shows no relief on the basement (modified from Haid/ et al.. in press). ;:,c "' s:, ""'s:, -~ ..,.. :::,' ,2" ~ "" ~ l;""" 51°00' .. - -·- ~ 22 "' :,~ "'~·· 0 +i: f;::; · c. ~ :E :.,,, .,. 18 v, :::: - -· . c ~ -i -· ·\ .: .. ~\;>: ······ .. ... ·~·. " \ t ····\~~' • 17 ~ ·"",,:: .\ \. •. \ .. .·, :::::·::-:-::. +-:::::-:-::.·.. \ · + r-- r 16 ·+ .·, l : 15

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27 26 25 49°00' 6 1 Range W2 102°00' W1 Areas of Red River MONTANA I NORTH DAKOTA production • Lighting Creek Structure & Workman Structure ..., * ..... situatedFigure 12 within • Deadwood these areas. isopach Contou mapr showinginterval isnortheast- 20 ,n and north west-trending elongate area.r ofthi nning over basement highs. Note that nwny of the Red River pools are 4. Stratigraphy In southeastern Saskatchewan, the basal unit of the Bighorn Group is termed the "Red River" and is formally subdivided into an upper formation, the Herald, and a lower, the Yeoman, (Kendall, l 976) (Figure 3). Where this subdivision cannot be recognized on geophysical logs, Red River Fonnation is used (Kreis and Haid!, 2000). In the U.S. portion of the Williston Basin (Figure 2), the term Red River Fonnation is used, and is further subdivided into drilling-based informal intervals called the "A", "B" and "C" in descending order (Longman and Haid!, 1996).

The Herald and Yeoman fonnations are Late (Edenian, Maysvillian, and Early Richmondian) in age (Elias et al., 1988; Norford et al., 1994 ). In southeastern Saskatchewan, the Yeoman generally overlies shales of the Icebox Member of the Winnipeg Fonnation (Trentonian-Early Edenian). The Figure I 3 - Ellrthqu"ke map showing northwesterly and nature of the contact is uncertain. Paterson ( 1971) northeasterly linear trends in the Williston Basin, interprets this contact to be erosional, at least in part, at rnutheastern Saskatchewan and the conterminous United the margins of the Winnipeg depositional basin. Other Stutes (from Earth Physics Branch, C"nada Department of workers believe that the contact is conformable and Energy, Mines and Resource.{, Victoria, Briti.~h Columbia, merely represents a depositional hiatus (Vigrass, 1971; 1977, in Mollurd, 1987). Ellingson and LeFever, l 995; Le Fever, 1996; Kreis, 2000b). In extreme southeastern Saskatchewan, beds of calcareous shale belonging to the Rough lock Member,

r .. the uppermost member of the Winnipeg Fonnation, are • less than 5 m thick. Th is unit thickens to the south into c North Dakota (Figure 15). The Upper Ordovician ,,,B ! I (Late Richmondian in age) .J_,. I ... overlies, with nondepositional discontinuity, the Herald - ,. in southeastern Saskatchewan (Kendall, 1976). ' ' ·w··-,- •· - •· ' ·-~ The Yeoman Fonnation is made up of totally "•'Oft ,f('!lon1 X· X or,dV-"I" ·- dolomitized, partially dolomitized and nondolomitized, burrow-mottled and burrowed but nonmottled, lime mudstones and wackestones with scattered packstone and grainstone lenses of skeletal debris (Porter and Fu Iler, 1959; Kendall, 1976; Canter, J 998; Kent and Haid!, 1999). The skeletal debris most commonly

PLAN observed in core is brachiopod valve fragments, crinoid columnals, and scattered solitary rugose corals. Much of the debris is so finely comminuted that it is only recognizable in thin section. However, recent cores of the Yeoman from the Tyvan, Montmartre, and Chapleau Lake areas have much coarser skeletal debris including hormotomid and bcllerophonid gastropods, catenoporid and favositid corals, well preserved

Souris Velie FIQOr brach iopod valves, and orthocone fragments. In

LONGIT'JOINAL PROFILE general, the Yeoman can be subdivided into a lower interval mainly made up of limestone and an upper interval, variably composed of limestone and Figure 14 - Profile amt plan views ofpart ofthe Souris dolostone. According to Kent and Haid! ( 1999), the River Valley showing changes in morphology, possibly upper Yeoman is predominantly dolostone east of a related to active tectonism, west of Estevan, southeastem line running from 17-32Wl to I-IOW2. West of that Saskatchewan (from Mo/lard, 1987). line, within the study area, apart from a few exceptions such as the Husky Cedoux 5- l l- l l- I 4W2 well in Froid-Fromberg fault zone (Figure 2), implying they which the upper interval is totally dolomitized, the are genetically related. upper Yeoman has alternating limestone and dolostone intervals. Favourably dolomitized zones in this upper interval arc the primary oil reservoirs in Yeoman rocks in southeastern Saskatchewan.

34 Summary o/lnvesligatlons 2000. I "olr1me I The basal interval of the Lake c C' Alma Member is not easily SASKATCHEWAN NORTH DAKOTA identified on geophysical well logs but is recognizable in core, IMPERlAL HALKETT SVANGSlU NO. 2+18 Kent and Kissling ( 1998) 15-7-3-8W2 SE/SWt3-1~ demonstrated that it contains G G S D significant facies variations, MIDDLE which they considered to ASHERN represent pronounced shallowing of the below-fair-weather wave base conditions that prevailed during Yeoman time. They defined four basic facies - oolitic shoals, stromatoporoid- UPPER m icrobialitic banks, shallow­ INTER LAKE water open-marine, and tidal flats - using textural, biotal, and allochem ic criteria (Figure 16).

The oolitic shoals are composed of dolo-packstones and dolo­ grainstones of 0.15 to 0.5 mm, LOWER INTERLAKE ovoid to elongate, ooids with single outer cortices coating pale STONEWALL yellowish grey dolomicritic nuclei. The thickest deposits of STONY MTN. ooids lie along I 02°W where they reach almost 3 m in thickness. Elsewhere beds arc seldom more than 0.5 m thick and are a:: commonly interlayered with 0.1 uJ > to 0.2 m thick oolitic and skeletal ii wackestones and YEOMAN D wackepackstones, The skeletal ~ I ORDOVICIAN debris mixed with the ooids is i thin-she] led brach iopod valve fragments and crinoid columnals . ('.) ICEBOX__j ~ with rare calcareous algae disks ,z and ramose bryozoan fragments. BLACK ISLAND ' ~ The strom atoporo id-microbial i tic bank facies is best developed in the L YR et al. Steelman 7-28-4- 4 W2 wel I where the sequence comprises: I) a rudstone unit DEADWOOD (4.4 m thick) dominated by Jam inar stromatoporoids; 2) a reefal boundstone (2.8 m thick) composed primarily of ' ''digitate and locally crust-like PRECAMBRIAN I PREC~BRIANl 'thromboids' of microbial origin"; and 3) two thin (each Jess Figure 15 - Two well cross-section C-C' (see Figure I) showing correlation of Lower than I m) skeletal beds which Paleozoic strata between southeastern Saskllfchewan and northwestern North Dakota. were deposited at the top of the The Herald Formation is composed of , sequence, and between the dolostones, and evaporites. It is subdivided in rudstone and the overlying microbial boundstone (Pratt ascending order into the Lake A Ima and Coronach et al., 1996 ). In addition to laminar stromatoporoids and thromboids, fossil components include domical members and the Rcdvers unit (Kendall, 1976). The Lake Alma Member is lithologically the most varied stromatoporoids, crinoid columnals, trilobite and bra ch iopod fragments. rugosc corals, ostracodes, unit of the entire Red River succession. It includes an upper anhydrite, the Lake Alma Anhydrite. a medial ramose bryozoans, gastropods and calcareous algae (Ort one/la). laminated to bedded dolomitic unit, the "C" Laminated. and a basal interval with a variety of carbonate facics. The shallow-water, open-marine rocks are dominated by skeletal and/or l'/ano/i1es-burrowed dolom icrites

Suska1c/1ewu11 Cieo!og1ca! S11n•e_1· 35 104° 103° 102°

6

4

2 49° 19 17 15 13 11 9 7 5 3 33 31 ~Oolitic Grainstone ~ Tidal flat ~ Strom bank

Figure 16- Basal lake Almafacies map. and dolo-wackestones with, in places, fining-upward The "C" Laminated interval of th e Lake Alma Member intervals of dolo-packstone and dolo-grainstone. The is both laminated and thinly bedded. Hairline solution skeletals include crinoid columnals, solitary coral seams commonly accentuate the interlaminar surfaces debris, brachiopod valve fragments, broken ramose and bedding planes. In places, the laminations arc bryozoa, wafer-like fragments of stromatoporoid, and stromatolitic in appearance. Elsewhere, sharp oncolite-coated nautiloid debris. Between the oolitic discontinuities are present. above which are elongate, shoals, the open-marine sediments are commonly flat intraclasts. Most layers are made up of extremely disturbed and distorted dolomicrites with pods and finely crystalline dolomicrite sufficiently dense that streaks of ooids. conchoidal fractures are produced on broken surfaces. Ostracod remains are generally the only fossils found, Tidal-flat deposits are represented by alternating light­ but typical stenohaline biota have been seen in a few and dark-coloured, planar, wavy and crinkly laminated widely distributed cores, including crinoid columnals, dolomicrites in which some of the laminae are brachiopod valve fragments, solitary rugose corals, discontinuous whereas others appear to have been bryozoans, and calcareous algae disks. broken into granule- and pebble-size clasts. Some laminae have planar surfaces, others have wavy upper The generally dense character of the "C" Laminated or lower surfaces. Bu lges on an upper surface of one gives the rock poor reservoir potential, but one of the lamina are commonly compensated for by indentations most prolific o il producers of the prc- 1995 wells, CDR in the bottom surface of the overlying layer. These S Lake Alma l-1 4-l-1 7W2, produced fr om this unit. In rocks are similar to those illustrated by Demicco and addition, Tri-Link Tyvan I0-1 7-1 3-13W2 is strongly Hardie (1994) and interpreted to have had a tidal-flat oil-stained in the "C" Laminated which here appears to origin . be the best interval for potential hydrocarbon production. Thin-section studies by Kent and Haid I ( I 999) show the do lorn ite of th e reservoir rock in 1-1 4-

J{j Summary of !m·l.'stigatio11s 2000, J 'ofume I 1- l 7W2 is more coarsely crystalline than normal. Kent wackestone and an upper dolomicrite. The skeletal (1997) records the presence of highly dolomitized lime mudstone to wackcstone is poorly to non­ skeletal debris in the thin sections which could account stratified, dominantly cryptocrystalline, but in places for the coarser crystallinity of the dolomite. microcrystalline, limestone with abundant solution seams and rare burrow and burrow-halo networks. The The Lake Alma Anhydrite is equivalent to the "C" main allochems are crinoids, brachiopod and ostracod Anhydrite in the U.S. part of the Williston Basin. It is valve fragments, and rugose corals. Where it is cored, the most extensive of the evaporites found in the the dolomicrite is similar to the "C" Laminated, and Herald Formation. In Canada, it extends a few ranges varies from laminated to thinly and thickly bedded. into Manitoba, as far north as Township 33 and to Elsewhere, the dolomicritic interval also has some well Range l OW3 in western Saskatchewan (Kent, 1960; developed stromatolites, particularly close to the Kendall, 1976; Norford et al., 1994; Kreis and Haid!, stratigraphic level of the Coronach Anhydrite. The 2000). The Lake Alma Anhydrite is partially or totally entire Coronach section is dolomitized in two cores. In cored in 20 wells. Its contact with the overlying other cores, only the dolomicrite and the upper few Coronach Member is generally placed at the base of a metres of the skeletal lime mudstones and wackestones thin laminated dolomicrite which passes upward into are dolomitized. the nodular limestones of the basal Coronach. In places, the laminated dolomicrite is absent and the The Redvers unit is dominantly bedded to laminated, contact is at the base of the limestone. On geophysical poorly fossiliferous lime mudstone and dolomicrite. It well logs this contact is located at the base of a slight is, however, markedly different in core from CDN­ increase in the gamma-ray signature. DEV TW Langbank 15-28-12-2W2, where it is a brachiopod-rich wackestone with a thin oolitic The Lake Alma Anhydrite typically has a layered grainstone at the base. appearance due to either interlaminated anhydrite and dolomite or inherent bedding in the anhydrite. Where dolomite is present, it may be in the form of discrete millimetre-thick laminae or discontinuous streaks. In 5. Depositional History several cored wells the evaporite is split into two The Upper Ordovician Red River strata of the Bighorn anhydrite intervals by about a metre of laminated Group record deposition of marine carbonate rocks in a dolomicrite, and the lower portion is nodular rather clear-water sea. The basal contact between the marine than layered. carbonates of the Yeoman and the underlying marine shales of the Winnipeg is relatively sharp, suggesting a The Coronach and Redvers are equivalent to the "B" rapid change in the depositional regime of the and lower "A" zones in the U.S. portion of the Williston Basin during this transition. The monotonous Williston Basin (Figure 3 ). To date, neither of these succession of burrow-mottled and mainly lime mud­ units is considered to have much hydrocarbon­ supported sediment implies low-energy conditions producing potential in Saskatchewan. However, in through most of Yeoman time, but, in places, thin light of exploration successes in the "B" zone of storm sheets made up of skeletal grainstones and Bowman County, North Dakota, and the Buffalo Field, packstones punctuate the succession and are indicative South Dakota, they should not be totally overlooked. of intermittent higher energy conditions. The presence Also, scattered oil shows occur in the Coronach of horizontal to oblique burrow mottles in the Yeoman Member in some of the 17 cores in southeastern Formation suggests the sediments were below fair­ Saskatchewan. In eight of these cores, the complete weather wave base (Kendall, l 976). An apparent lower Coronach succession is present. The Redvers is fully diversity of biota in the Yeoman in southeastern cored in four wells and part of it is present in another Saskatchewan than in east-central Saskatchewan and three cores. western Manitoba led Kendall (1976) to argue that deeper water conditions prevailed there. He supported The Coronach-Redvers contact is intersected in nine his proposal with reported occurrences of ripple marks cores, in four of which it is easily determined as it is and desiccation cracks in the Red River outcrops of placed at the top of either the Coronach Anhydrite or a east-central Saskatchewan. If his argument is valid, patterned carbonate above the evaporite. The evaporite slight increases in biota! diversity in the Yeoman is absent or poorly preserved in five cores, and the reported for the Montmartre and Tyvan areas may contact is placed at a sharp, readily recognizable indicate local shoaling in southeast Saskatchewan. bedding surface that is overlain by an intraclastic breccia. No obvious brecciation is present in the fifth The basal Lake Alma represents shallowing prior to core in which the contact is located at the top of a restriction of the sea, leading to the accumulation of bedded to laminated dolomicritic interval. On penesaline rocks of the "C" Laminated and the geophysical logs, the contact is placed at the base of an hypersaline Lake Alma Anhydrite. The normal-marine, increase in gamma radiation that, in places, shows as a shallow-water setting represented by the thin basal sharp positive deflection of the gamma-ray curve about Lake Alma rocks presents the most varied facies 3 to 5 m below the base of the Hartaven Member of the relationships found in the Bighorn Group. The Stony Mountain formation. Aside from the thinly overlying Coronach replicates the Yeoman-Lake Alma laminated dolomicrite at its base and a thinly layered succession except an equivalent to the basal Lake Alma anhydrite at the top, the Coronach is composed of two interval is absent. The top of the Coronach may other lithologies, a lower skeletal lime mudstone to represent an important hiatus. lntraformational breccias

Saskatchewan (ieo!og1cul Survey 3 7 are present in four wells, two of which are in the at these localities. The biota contrast with thinner­ Midale area, that intersect the Coronach-Redvers valved brachiopods and an absence of colonial corals contact. This contact in one of the Mi dale wells, I 2-2- in Yeoman cores taken at some distance from the 7-11 W2, is an irregular surface underlain by a mosaic highs. A possible subaerial exposure surface is present breccia of flat clasts O. I to I cm in diameter. It is at the top of the Coronach in Midale 12-2-7-11 W2, overlain by ovoid, rounded clasts of similar diameter to also located over a basement high. those in the mosaic breccia supported in an argillaceous dolomicritic matrix. The combination of Not every basement structure was reactivated during mosaic breccia in the rocks underlying the contact and the time of Bighorn deposition. This is shown by the the irregularity of the surface suggests a possible presence of highs over which the Red River is not subaerially exposed surface. The Redvers is anomalously thin. At these locations, basal Lake Alma predominantly laminated to bedded and may represent lithotypes are typically dolo-wackestones and a penesaline environment similar to that represented by dolomicrites with thin-valved brachiopods. Also, not the laminated facies near the base of the Lake Alma. al\ localities with thin Red River have high-energy lithotypes. For example, cores from wells in the area covered by Townships l to 12 and Ranges 12 to 21 west of the second meridian have tidal-flat rocks in the 6. Structural Controls on Sedimentation basal Lake Alma. Nonetheless, the occurrence of Kent(] 987) compiled information about structural grainstones and packstones in basal Lake Alma cores controls on sedimentation from many sources. He used commonly suggests an underlying basement high. localized thinning and thickening of marker-defined intervals as evidence for syn-depositional tectonic The localized nature of oolite occurrences at Chapleau activity. He also identified localities where anomalous Lake, Tyvan, Montmartre and Midale questions the occurrences of rocks that were originally deposited in existence of the extensive oolitic shoal identified by shallower or deeper water could be attributed to Kent ( 1960) and Kendall ( 1976) in an area close to seafloor features resulting from synsedimentary 102°W. Oolite grainstones in cores from this area can structural up- or down-warping. Similarly, this study alternatively be interpreted as being located on attempts to identify structurally controlled isolated, structurally positive features. As a broad sedimentation in the Bighorn Group. The shallow­ regional Precambrian high (Figure 7) appears to be water sediments of the basal Lake Alma are an obvious present, however, we prefer the extensive oolitic shoal interval to study for anomalous facies developments as interpretation (Figure 16). they would have more sensitively reflected bathymetric changes than the deeper water sediments of the Yeoman. Anomalous facies developments coincident 7. Economic Considerations with anomalous thinning or thickening of a stratigraphic interval provide evidence for syn­ To date, all Red River hydrocarbon production in depositional structural control (neither criterion alone southeastern Saskatchewan appears to be underpinned is firm evidence for such control). by Precambrian basement with measurable positive paleotopographic relief. Producing wells which Three of the maps presented here are significant to this penetrate the basement invariably show some thinning study. The Deadwood isopach map (Figure 7) and the or complete absence of the overlying Deadwood Precambrian structure map (Figure 9) demonstrate the Formation. The assumption therefore appears existence of Precambrian basement paleotopographic reasonable that wells which do not penetrate the highs in southeastern Saskatchewan. The Red River Precambrian, but show Red River hydrocarbon isopach map (Figure 8) shows thinning over some of entrapment, are likely to overlie a basement high. The these features, a commonly recorded characteristic apparent orthogonal arrangement of basement highs elsewhere in the basin (Byrd, 1978; Martens, 1978; recognized from isopach mapping of the Deadwood Mueller and Klipping, 1978; Sharp, 1978). This and similar panems from lineament mapping may thinning can be anributed to syn-depositional upward prove useful as trend indicators for future plays of this movement of the reactivated basement highs. The basal type. Lake Alma in core from wells located over basement highs in the Chapleau Lake, Tyvan, Montmartre, and Generally, structural highs on the Precambrian surface Midale areas is made up of oolitic dolo-grainstones and (Figure 9) show up as structural highs on the top of the dolo-packstones (Figure 16). Stromatoporoid­ Red River (Figure I 0) suggesting a genetic microbialitic banks occur over a high in the Weir Hill relationship. Also, hydrocarbon production is generally area, as do parts of tidal-flat complexes in the Ceylon greater over the structurally highest Red River area (Figures l and 16). In contrast, basal Lake Alma locations which tend to coincide with relatively higher cores from wells that are close to, but not over paleotopographic relief on the basement. Bearing this basement highs, have ooids in dolo-wackestones and in mind, the Amerada Crown S AD 13-12-14-24 W2 dolomicrites. From more distally located wells, they well location, which shows the highest positive relief are generally skeletal wackcstones and lime on the Precambrian basement yet recognized from mudstones. Yeoman wackestones containing favositid mapping in southeastern Saskatchewan, is highly and cateniporid corals and thick-shelled, robust prospective (Figures 7, 9, and 10). The Yeoman brachiopods in core from Chapleau Lake, Tyvan, and portion of the Red River was not drillstcm tested in this Montmartre may also subtly reflect shallower seatloor well, and evaluations of the SP, resistivity, gamma-ray

38 Summary oflnvestigalions 2000, J 'olumc I and neutron logs taken in 1958 are inconclusive. Cores 9. Acknowledgments were not taken but cuttings show some zones of porosity and oil stains within the Stony Mountain The authors gratefully acknowledge Phil Weir and Erik Formation and the upper portion of the Yeoman Nickel for their assistance in the preparation of figures Formation. Fluorescence micro-spectrometry studies for this paper. suggest that the stains contain 3 0° to 35° AP! oil. Optical data from reflectance and fluorescence analysis of macerals in kukersitic source rock intervals 10. References associated with the stained cuttings show that the macerals are thermally immature to marginally mature. Andrichuk, J.M. (1959): Ordovician and Silurian The oil found in this well has, therefore, probably stratigraphy and sedimentation in southern migrated from a mature, downdip source (L.D. Stasiuk, Manitoba; Amer. Assoc. Petrol. Geo!. Bull., v43, pers. comm., 2000). p2333-2398.

Kent ( 1973), using the isopach map from Ballard Baird, D.J., Nelson, K.D., Walters, J.J., and Brown, ( 1969), recognized that most Ordovician producing L.D. ( I 995): A comparison of crustal structure areas from the U.S. portion of the basin were along strike in the Trans-Hudson Orogen from associated with anomalously thin Upper Red River LITHOPROBE and COCO RP transects; in Hajnal strata. This is also demonstrated by Byrd ( 1978), Z. and Lewry, J. (eds.), LITHOPROBE Trans­ Martens (1978), Mueller and Klipping (1978), and Hudson Orogen Transect, Rep. No. 48, p47-65. Sharp ( 1978). Recent mapping further corroborates this association. The Red River also shows subtle thinning Ballard, W.W. (1969): Red River of northeast Montana in the Amerada Crown SAD 13-12-14-24W2 well and northwest North Dakota; Mont. Geo!. Soc., (Figure 8), suggesting the prospect of a nearby trap. East. Mont. Symp., pl5-24.

Identification of concentrations of oolitic or Bell, J.S. and Babcock, E.A. ( 1986): The stress regime stromatoporoid-microbialitic bank facies in wells that of the Western Canadian Basin and implications do not penetrate Precambrian basement might be for hydrocarbon production; Bull. Can. Petrol. indicative of an area close to or overlying a Geo!., v34, p364-378. Precambrian basement high. A secondary indicator may be the presence of coarse skeletal remains of Bell, J.S., Price, P.R., and McLellan, P.J. (1994): In­ catenoporid or favositid corals, thick-shelled situ stress in the Western Canada Sedimentary brachiopods and high-spired gastropods. Recognition Basin; in Mossop, G. and Shetsen, I. (comp.), of these basement features may help focus exploration Geological Atlas of the Western Canada efforts. Sedimentary Basin; Can. Soc. Petrol. Geol./Alta. Resear. Counc., p439-446. Basement features have been linked to heat flow and electric conductivity anomalies in southeastern Brown, D.L. and Brown, D.L. ( 1987): Wrench-style Saskatchewan (Majorowicz et al. , 1988). Improved deformation and paleostructural influence on knowledge of these anomalies and their apparent sedimentation in and around a cratonic basin; in source in the Precambrian basement will enhance our Longman, M.W. (ed.), Williston Basin: Anatomy understanding of the thermal maturation, migration and of a Cratonic Oil Province, Rocky Mtn. Assoc. accumulation of Red River and other oils in southeast Geol., Denver, µ57-70. Saskatchewan. Exploration successes in the Red River and the Winnipeg Formation over the past few years Burwash, R.A., Green, A.G., Jessop A.M., and should provide an economic incentive to pursue this Kanasewich, E.R. ( 1993): Geophysical and work. petrological characteristics of the basement rocks of the Western Canada Basin; in Stott, D.F. and Aitken, J.D. (eds.), Sedimentary Cover of the 8. Future Work Craton in Canada, p55-77. Staff of the Petroleum Geology Branch, in Byrd, W.J. (1978): Geology of the Mondak West and collaboration with colleagues from the Northern Mondak fields in Richland County, Montana and Geological Survey Branch of Saskatchewan Energy McKenzie County, North Dakota; in Estelle, D. and Mines, plan to continue investigating the sub­ and Miller, R. (eds.), Williston Basin Symposium Phanerozoic Precambrian basement and its features. Guidebook, Mont. Geo!. Soc., p307-3 I l. They have recently completed regional subsurface mapping of the province's Lower Paleozoic formations Canter, K.L. (1998): Facies cyclostratigraphic and and will next map the Devonian strata. secondary diagenetic controls on reservoir distribution, Ordovician , Midale Field, southern Saskatchewan; in Eighth International Williston Basin Symposium, Core Workshop Volume, Sask. Geo!. Soc., p41-66.

Saskatchewan Geofogical Survey 39 Christopher, J.E. ( 1961 ): Transitional Devonian­ Gerhard, L.C., Anderson, S.B., and Fischer D.W. Mississippian Fonnations of Southern (1991 ): Petroleum geology of the Williston Basin; Saskatchewan; Sask. Dep. Miner. Resour., Rep. in Leighton, M.W., Kolata D.R., Oltz D.F., and 66, 103p. Eidel J.J. (eds.), Interior Cratonic Basins, Amer. Assoc. Petrol. Geol., Mem. 51, p507-560. - ~-- -(1980): The Lower of Saskatchewan - a tectonic over-view; in Gibson, R.1. ( 1995): Basement tectonics and Beck, L.S., Christopher, J.E., and Kent, D.M. hydrocarbon production in the Williston Basin: An (eds.), and Beyond: Geology of interpretive overview; in Hunter, L.D. and Schalla, Mannville Hydrocarbon Reservoirs, Sask. Geol. R.A. (eds.), Seventh International Williston Basin Soc., Spec. Publ. No. 5, p3-32. Symposium, Sask. Geol. Soc., Spec. Publ. No. 12, p3-9. Crowley, K.D., Ahem, J.L., and Naeser, C. W. (1985): Origin and epeirogenic history of the Williston Gough, D.I. and Bell, J.S. ( l 981 ): Stress orientations Basin: Evidence from fission-track analysis of from oil-well fractures in Alberta and Texas; Can. apatite; Geo!., vl3, p620-623. J. Earth Sci., v 18, p638-645.

Demicco, R.V. and Hardie, L.A. (1994): Sedimentary Green, A.G., Hajnal, Z., and Weber, W. (1986): An Structures and Early Diagenetic Features of evolutionary model of the western Churchill Shallow Marine Carbonate Deposits; Soc. Econ. Province and western margin of the Superior Paleont. Mineral., Atlas Series No. 1, 265p. Province in Canada and the north-central United States - reply; Tectonophys., v 131 , p I 88-197. Dickinson, W.R. ( 1976): Plate tectonic evolution of sedimentary basins; in Dickinson W .R. and Green, A.G., Weber, W. , and Hajnal, Z. (1985a): Yarborough H. (eds.), Plate Tectonics and Evolution of Proterozoic terrains beneath the Hydrocarbon Accumulations, Amer. Assoc. Petrol. Williston Basin; Geol. , v 13 , p624-628. Geo!., Continuing Education Course Notes, Series 1, pl-56. _ _ _ _ _ (1985b): An evolutionary model of the western Churchill Province and western margin of Dietrich, J.R. and Magnusson, D.H. ( 1998): Basement the Superior Province in Canada and the north­ controls on Phanerozoic development of the central United States; Tectonophys., v 116, p28 l- Birdtail-Waskada salt dissolution zone, Williston 322. Basin, southwestern Manitoba; in Christopher, J.E., Gilboy, C.F., Paterson, D.F., and Bend, S.L. Haid!, F.M., Kreis, L.K., Miles, W., Nickel, E., and (eds.), Eighth International Williston Basin Ware, M.J. (in press): Relationships between Symposium, Sask. Geol. Soc., Spec. Publ. No. 13, Phanerozoic sedimentation, erosion, hydrocarbon p166-l 74. accumulations and basement tectonics: Examples from Lower Paleozoic strata in southeastern Elias, R.J., Nowlan, G.S., and Bolton, T.E. () 988): Saskatchewan; Geocanada 2000 abstracts. Paleontology of the type section, Fort Garry Member, Red River Fonnation (Upper Holter, M.E. (1969): The Middle Devonian Prairie Ordovician), southern Manitoba; in Wohlberg, Evaporite of Saskatchewan; Sask. Dep. Miner. D.L. (ed.), Contributions to Paleozoic Resour., Rep. 123, I 34p. Paleontology in Honor of Rousseau H. Flower, New Mexico Bur. Mines and Miner. Resour., Jones, A.G. and Savage, P.J. ( 1986): North American Mem. 44, p341-359. Central Plains conductivity anomaly goes east; Geophys. Resear. Lett., v 13, p685-688. Ellingson, J.B. and Lefever, R.D. (1995): Depositional environments and history of the Winnipeg Group Kendall, A.C. ( 1976): The Ordovician Carbonate (Ordovician), Williston Basin, North Dakota; in Succession (Bighorn Group) of Southeastern Hunter, L.D. and Schalla, R.A. (eds.), Seventh Saskatchewan; Sask. Miner. Resour., Rep. 180, International Williston Basin Symposium, Sask. 185p. Geo!. Soc., Spec. Publ. No. 12, pl29-139. Kent, D.M. (1960): The Evaporites of th e Upper Fowler, C.M.R. and Nisbet, E.G. (1985): The Ordovician Strata in the Northern Part of the subsidence of the Williston Basin; Can. J. Earth Williston Basin; Sask. Dep. Miner. Resour., Rep. Sci., v22, p408-4 I 5. 46, 46p.

Gerhard, L.C., Anderson, S.B., Lefever, J.A., and -~~~- ( 1973): Paleozoic hydrocarbon reservoirs Carlson, C.G. (1982): Geological development, in Saskatchewan and their relationship to origin, and energy mineral resources of the basement lineaments; J. Can. Petrol. Tech., v 12, Williston Basin; Amer. Assoc. Petrol. Geol. Bull., p20-24. v66, p989-I 020. - ~ ~ - - ( 1974): Relationship between hydrocarbon accumulations and basement

40 Summwy of In vestigations 2000, Volume I structural elements in the northern Williston Basin; Kreis, L.K., Ashton, K. E., and Maxeiner, R.O. (2000): in Parslow, G.R. (ed.), Fuels: A Geological Geology of the Precambrian basement and Appraisal, Sask. Geol. Soc., Spec. Publ. No. 2, p3- Phanerozoic strata in Saskatchewan; Sheet I of 8, 80. Lower Paleozoic Map Series, Sask. Energy Mines, Open File Rep. 2000-2. --~ -- ( 1987): Paleotcctonic controls on sedimentation in the northern Williston Basin, Kreis, L.K. and Haid!, F.M. (2000): Geology of the Saskatchewan; in Longman M. W. (ed.), Williston Upper Ordovician Red River strata (Herald and Basin: Anatomy ofa Cratonic Oil Province, Rocky Yeoman formations) in Saskatchewan; Sheet 4 of Mtn. Assoc. Geo!., Denver, p45-56. 8, Lower Paleozoic Map Series, Sask. Energy Mines, Open File Rep. 2000-2. _ _ _ _ _ (1997): Lithologics and reservoir characteristics of Ordovician Red River cycles, Lefever, R.D. ( 1996): Sedimentology and stratigraphy southeastern Saskatchewan; D.M. Kent Consulting of the Deadwood-Winnipeg interval (Cambro­ Geologist Ltd., Regina, unpubl. rep. Ordovician), Williston Basin; in Longman, M.W. and Sonnenfe ld, M.D. (eds.), Paleozoic Systems of Kent, D.M. and Christopher, J.E. (1994): Geological the Rocky Mountain Region, Rocky Mtn. Sec., history of the Williston Basin and Sweetgrass Soc. Econ. Paleont. Mineral., p 11 - 18. Arch; in Mossop, G.D. and Shetsen I. (comp.), Geological Atlas of the Western Canada Lewry, J.F. and Collerson, K.D. (1990): The Trans­ Sedimentary Basin, Can. Soc. Petrol. Geol./Alta. Hudson Orogen: Extent, subdivision, and Geol. Surv., p421-430. problems; in Lewry, J.F. and Stauffer, M.R. (eds.), The Early Proterozoic Trans-Hudson Orogen of Kent, D.M. and Kissling, D.L. ( 1998): Covert facies of North America, Geo!. Assoc. Can., Spec. Pap. 37, the Red River C laminated member, northern pl- 14. Williston Basin; in Christopher, J.E., Gi lboy, C.F., Paterson, D.F., and Bend, S.L. (eds.), Eighth Longman, M.W. and Haid!, F.M. (1996): Cyclic International Williston Basin Symposium, Sask. deposition and development of porous dolomites Geo!. Soc., Spec. Publ. No. 13, p24. in the Upper Ordovician Red River Formation, Williston Basin; in Longman, M.W. and Kent, D.M. and Haidl, F.M. ( 1999): Depositional Sonnenfeld, M.D. (eds.); Paleozoic Systems of the Environments and Reservoir Potential of Lower Rocky Mountain Region, Rocky Mtn. Sec., Soc. and Middle Paleozoic Rocks in Saskatchewan; Econ. Paleont. Mineral. , p29-46. unpubl. notes for CSPG Short Course G-4 Can. Soc. Petrol. Geol. and CIM Petrol. Soc. Macdonald, R. and Broughton, P. ( 1980): Geological Conference, Calgary, I 09p. Map of Saskatchewan; Sask. Dep. Miner. Resour., 1: I 000 000 scale map, provisional edition. Kissling, D.L. ( 1997): Rethinking the configurations of Red River reservoirs; Fifth International Williston Majorowicz, J.A., Jones, F.W., and Jessop, A.M. Basin Horizontal Well Workshop Notes, Sask. ( 1986): Geothermics of the Williston Basin in Energy Mines/N. Dakota Geol. Surv., 9p. Canada in relation to hydrodynamics and hydrocarbon occurrences; Geophys., v5 I , p767- Kohm, J .A. and Louden, R.O. ( 1978): Ordovician Red 779. River of eastern Montana-western North Dakota - relationships between lithofacies and Majorowicz, J.A., Jones, F.W., and Osadetz, K.G. production; in Estelle, D. and Miller, R. (eds.), (1988): Heat fl ow environment of the electrical Williston Basin Symposium Guidebook, Mont. conductivity anomalies in the Williston Basin, and Geol. Soc., p99-l 17. occurrence of hydrocarbons; Bull. Can. Pet. Geo!., v36, p86-90. Kreis, L. K. ( 1991 ): Stratigraphy of the System in the Wapella-Moosomin Area, Southeastern Martens, R. W. (1978): Boxcar Bune, North Dakota; in Saskatchewan; Sask. Energy Mines, Rep. 2 17, Estelle, D. and Miller, R. (eds.), Williston Basin 90p. Symposium Guidebook, Mont. Geol. Soc., p327- 344. - ~ -~ (2000a): Geology of the Middle Cambrian- Lower Ordovician Deadwood McCabe, H.R. ( 1967): Tectonic framework of Formation in Saskatchewan; Sheet 2 of 8, Lower Paleozoic formations in Manitoba; Trans. Can. Paleozoic Map Series, Sask. Energy Mines, Open Inst. Min. Metal., v70, pl80-189. File Rep. 2000-2. Miles, W.F., Roest, W.R., Kelley, L, and Gent, M.R. ~ --=---c-- _ (2000b): Geology ofthe Middle (2000): Rationalized detailed gravity data, Ordovician Winnipeg Formation in Saskatchewan; southern Saskatchewan, Geol. Soc. Can. Open File Sheet 3 of 8, Lower Paleozoic Map Series. Sask. Rep. 03883/Sask. Energy Mines Open File Rep. Energy Mines, Open File Rep. 2000-2. No. 2000-1, CD-ROM .

.'',askalchewan Geological Survey 4/ Milkereit, D.W.E, Ross, G.M., Kanasewich, E.R., Geis, Penner, L.A. and Mollard, J.D. (1 99 1): Correlated W., Edwards, D.J., Kelsch, L. , and Yarsek, J. photolineament and geoscience data on eight ( 1995): LITHOPROBE basin-scale seismic petroleum and potash study projects in southern profiling in central Alberta: Influence of basement Saskatchewan; Can. J. Remote Sensing, v 17, on the sedimentary cover; Bull. Can. Petrol. Geol. , p 174-184. v43, p6 5-77. Porter, J.W. and Fuller, J.G .C.M. (1959): Lower Misra, K.S., Slaney, Y.R., Graham, D., and Harris, J. Paleozoic rocks of northern Williston Basin; (1991): Mapping of basement and other tectonic Amer. Assoc. Petrol. Geol. Bull., v43, p 124-189. features using Seasat and Thematic Mapper in hydrocarbon producing areas of the Western Potter, D. and St. Onge, A. ( 1991 ): Minton pool, south­ Sedimentary Basin of Canada; Can. J. Remote central Saskatchewan: A model for basement­ Sensing, v17, pl37-151. induced structural and stratigraphic relationships; in Christopher, J.E. and Haid!, F.M. (eds.), Sixth Mollard, J.D. (1987): Remote Sensing for Petroleum International Williston Basin Symposium, Sask. Exploration and Exploitation in Saskatchewan; Geol. Soc., Spec. Publ. No. 11, p21-33. Sask. Energy Mines, Fuels Research Program, Tech. Rep. No. 5, 206p. Pratt, B.R., Bernstein, L.M., Kendall, A.K., and Haidl, F.M. ( 1996): Occurrence of reefal facies in Red - ~ - ---= (1988): First R.M. Hardy Memorial River strata (Upper Ordovician), subsurface Lecture: Fracture lineament research and Saskatchewan; in Summary of Investigations applications on the Western Canadian Plains; Can. 1996, Saskatchewan Geological Survey, Sask. Geotech. J., v25, p749-767. Energy Mines, Misc. Rep. 96-4, p147-152.

_ _ _ __ (1 999): Field Trip Guide Booklet, 52nd Quinlan, G. (1987): Models of subsidence mechanisms Can. Geotech. Conf., Regina, 26p. in intracratonic basins and their applicability to North American examples; in Beaumont, C. and Mueller, C.A. and Klipping, R.S. ( 1978): Geology and Tankard, A.J. (eds.), Sedimentary Basins and geophysics of Sioux Pass fi eld, Richland County, Basin-forming Mechanisms, Can. Soc. Petrol. Montana; in Estelle, D. and Miller, D. (eds.), GeoI., M em. I 2, p463-48 l. Williston Basin Symposium Guidebook, Mont. Geo!. Soc., p345-354. Sharp, R.W. ( 1978): Geology of the Vaux field area, Richland County, Montana; in Estelle, D. and Nelson, K .D., Baird, D.J., Walters, J.J., Hauck, M., Miller, R. (eds.), Williston Basin Symposium Brown, L.D., O liver, J.E., Ahem, J.L., Hajnal, Z., Guidebook, Mont. Geol. Soc., p355-360. Jones, A.G., and Sloss, L.L. (1993): Trans-Hudson Orogen and Williston Basin in Montana and North Sims, P.K., Peterman, Z.E., Hildebrand, T.G., and Dakota: New COCORP deep profiling results; Mahan, S. ( I 991 ): Precambrian basement map of Geol., v21 , p447-450. the Trans-Hudson Orogen and adjacent terranes, Northern Great Plains, U.S.A.; U.S. Geol. Surv., Norford, B.S., Haid!, F.M., Bezys, R.K., Cecile, M.P., Map 1-2214, 1: 1000000 scale. McCabe, H.R., and Paterson, D.F. (1994): Middle Ordovician to Lower Devonian strata of the Stauffer, M.R. and Gendzwill, D.J. ( 1987): Fractures in Western Canada Sedimentary Basin; in Mossop, the northern plains, stream patterns, and the G .D. and Shetsen, I. (comp.), Geolog ical Atlas of midcontinent stress field; Can. J. Earth Sci., v24, the Western Canada Sedimentary Basin, Can. Soc. pl 086-1097. Petrol. Geol./Alta. Resear. Counc., pl09-127. Stewart, J.H. (1972): Initial deposits in the Cordilleran Osadetz, K .G., Kohn, B.P., O' Sullivan, P., Feinstein, geosyncline: Evidence of a late Precambrian S., Hannigan, P.K., Everitt, R.A., Gilboy, C.F., (850 m .y.) continental separatio n; Geol. Soc. Bezys, R.K., and Stasiuk, L.D. ( 1998): Amer. Bull., v83, p1345-1360. Thermotectonics of the Williston Basin and environs: Variations in heat fl ow and hydrocarbon Thomas, G .E. ( 1974 ): Lineament-block tectonics: generation; in Christopher, J.E., Gilboy, C.F., Williston-Blood Creek Basin; Amer. Assoc. Paterson, D.F., and Bend, S.L. (eds.), Proceedings Petrol. Geol. Bull., v58, p I 305-1322. of the Eighth Internatio nal Williston Basin Symposium, Sask. Geol. Soc., Spec. Publ. No. 13, Vi grass, L. W. ( 197 1) : Depositional framework of the pl47-165. Winnipeg Formation in Manitoba and eastern Saskatchewan; in Tumock, A.C. (ed.), Paterson, D.F. (1971): The Stratigraphy ofthe Geosciences Studies in Manitoba, Geol. Assoc. Winnipeg Formation (Ordovician) of Can., Spec. Pap. No. 9, p225-234. Saskatchewan; Sask. Dep. Miner. Resour., Rep. 140, 57p.

42 Summary of lnvesli1<;atio11.1· 2000, Volume 1