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Stratigraphy and Depositional Environment of Lower San Andres Formation in Subsurface and Equivalent Outcrops: Chaves, Lincoln, and Roosevelt Counties, New Mexico1

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Stratigraphy and Depositional Environment of Lower San Andres Formation in Subsurface and Equivalent Outcrops: Chaves, Lincoln, and Roosevelt Counties, New Mexico1 The American As.sociation of Petroleum OeolosiJts Bulletin 'V. 73, No. II (November 1989), P.I307· 132S, II Fias., llllblc Stratigraphy and Depositional Environment of Lower San Andres Formation in Subsurface and Equivalent Outcrops: Chaves, Lincoln, and Roosevelt Counties, New Mexico1 L.A . ELLIO~andJ . K . VVARllEN 3 ABSTRACT dolomite/anhydrite transition, and the accumulation and preservation of thick subaqueous evaporites north of This paper establishes correlations from subsurface to the study area. outcrop and develops a depositional model for the lower Sao Andres Formation in New Mexico. Five cyclic carbonate-evaporite sequences, numbered consecutively INTRODUCTION upward as units 1, 2, 3, 4, and 5, were identified from measurement of approximately 1, 750 ft (534 m) of sec­ The middle Permian San Andres Formation is a regres­ tion in the Hondo Canyon area of Lincoln County and sive carbonate-evaporite sequence deposited on broad examination of approximately 400 ft (122 m) of core platforms and shelves in the Permian basin (Figure 1). In from six wells in the Levelland-Slaughter trend of Chaves the Northwestern shelf province of southeast New Mex­ and Roosevelt Counties. An idealized sequence consists ico and west Texas, the cyclic lower member is a major of open-marine, restricted subtidal, intertidal, and hydrocarbon reservoir. Producing fields on the shelf are supratidal facies capped by anhydrite (in the subsurface) concentrated along an east-west line known as the or an evaporite dissolution zone (in outcrop). Lateral Levelland-Slaughter trend (Figure 2A), which is named facies changes in outcrop indicate that the Pedernal after the two largest fields in Cochran and Hockley uplift provided a locus for emergent conditi~n s at low Counties, Texas. In this trend, hydrocarbons are trapped relative sea level stands through the deposition of unit 3. where porous dolomites pinch out updip into nonporous Units 4 and 5 are incomplete, highly variable sequences. facies. With this type of stratigraphic/diagenetic trap, Lateral facies changes are not present in outcrop, indica­ detailed knowledge of environmental patterns is essential ting that the Pedernal uplift exerted little influence on the to generate successful exploration and development deposition of these units. strategies. Preserved anhydrite cores capping P 1 and P 1 sequences The Levelland-Slaughter trend projects into outcrop (equivalent to units 4 and 5) range up to 15 ft (5 m) thick, west of Roswell, New Mexico, due to a regional eastward are relatively pure, commonly lack underlying intertidal/ dip (Figure 2A). The proximity of outcrop to the produc­ supratidal carbonates, and contain some gypsum ghosts, ing trend provides a unique opportunity to study the indicating that part of the anhydrite was deposited sub­ lower San Andres Formation using both field and sub­ aqueously. We present a depositional model involving surface data. The purpose of this paper is to (1) establish both subaqueous (salina) and subaerial (sabkha) deposi­ regional correlations from the subsurface to equivalent tion of the anhydrite. The model accounts for the purity outcrops in the Hondo Canyon area of eastern Lincoln and thickness of the evaporite caps, the rarity of sub­ County, (2) describe facies from both outcrop exposures aerial exposure features, variations in the nature of the and subsurface cores, and (3) develop a regional model of deposition for the lower San Andres Formation in south­ east New Mexico. Seven detailed sections totaling @Copyright 1989. The Amencan Associahon of Petroleum Geologists. All approximately I, 750 ft (534 m) were measured (Figure rights reserved. 1Manuscript received, April4, 1988; accepted, July 6, 1989. 2B). Approximately 400ft (122m) of core from six wells 2Laura E. Tillman, Chevron U.S.A. Inc., P.O. Box 599, Denver, Colorado within the trend were also examined (Figure 2A, Thble 1) 80201 . ~ational Centre for Petroleum Geology and Geophysics, G.P.O. Box 498, to enhance understanding of the depositional and dia­ Adelaide. South Australia 5001 . genetic features observed during outcrop study and to This paper is part of a Master's thesis written by the primary author and relate these features to production characteristics. accepted by the University of Texas at Austin, Austin, Texas. Arco Exploration and Production and Tenneco Oil Company funded the study. We thank Much has been written on the San Andres Formation. Sneider Exploration, the New MexiCO Bureau of Mines and M1neral Resources, Subsurface studies include Dunlap (1967), Gratton and Dan Engles of Tenneco Oil Company, and Jack Ahlen for allowing us to study cores In their possession. Well logs were obtained with permission from the Lemay (1969), Chuber and Pusey (1972), Thdd (1976), Permian Association, Roswell New Mexico. Phelps Anderson, owner, and Jay Pitt and Scott (1981), Bein and Land (1982, 1983), Posey, foreman of the Diamond A Cattle Company, granted us access to the Ramondetta (1982a, b), Kumar and Foster {1982), Hov­ field area. Mike Tillman, Rick Otto, and Shiner were invaluable field assistants. George Martinez, Glenda Jackson. and Mark Sarene drafted and revised ~9- orka (1983, 1987), Ward et al (1986), Bebout and Harris ures In their spare time. S. D. Hovorka, A. L. Folk, D. G. Bebout, P. M. Hams. ( 1986), Cowan and Harris ( 1986), Fracasso and Hovorka J. F. Sarg, A. Evans, F. E. Kottlowskl, and A. F. Broadhead critically reviewed (1986), Fisher and Hovorka (1987), Harris and Stoudt this wortt at various stages and we are grateful for their many helpful com· ments. (1988), and Major et al (1988). Most outcrop studies of 1307 1308 Stratigraphy and Depositional Environment, Lower San Andres Formation \ <-.\ ~- the Early Permian (Wolfcampian), the complex of --,.&.Y basins, platforms, and shelves collectively known as the c. J-:- Permian basin were fully developed (Figure I) (Galley, ' ' l I 1958; Hills, 1984). The Eastern, Northern and North­ western shelves formed a broad horseshoe around the northern Delaware and Midland basins. The Palo Duro l basin, although very shallow, was subsiding and accumu- ""'LO DURO BASIN . lating sediment throughout the Permian. The Matador arch, Roosevelt uplift, and Pedernal uplift were buried ARc~ positive features that influenced sedimentation during San Andres deposition (Milner, 1974; Cowan and Harris, 1986). During San Andres deposition, the Northwestern shelf was a very broad extensive shelf area and the site of car­ I bonate deposition. Shelf sediments were characterized by I repetitive and laterally extensive transgressive and regres- sive packages. These repeated sequences commonly are ~-- explained by glacial-eustatic sea level fluctuations and ' changing subsidence rates (Jacka et al, 1967; Silver and '" Todd, 1969; Meissner, 1972; Wanless, 1972; Fracasso and Hovorka, 1986), although tectonics and climatic changes also may have been contributing factors. Subsidence was occurring at rates to permit the shelf to remain shallow, and to permit the development of a low-angle (5° or less) shelf margin with no abrupt break in slope (Sarg and Lehmann, 1986). This shelf margin trended northeast­ southwest through the present-day Eddy and Lea Coun­ ties south and east of the study area (Silver and Todd, 1969). Figure 1-Major geologic features of Permian basin, west Texas and southeast New Mexico (after Fracasso and Hovorka, SAN ANDRES STRATIGRAPHY 1986; Silver and Todd, 1969; Broadhead, 1987). Location of study area is shown as shaded hachure area. The San Andres Formation is approximately 1,200 ft (366m) thick and includes all the beds between the top of the San Andres Formation have concentrated on the the Yeso Formation (Leonardian) and the base of the exposures in the Guadalupe Mountain area south of the Grayburg Formation (middle Guadalupian). In the study study area. Boyd (1958) and Hayes (1959, 1964) were the area, the lowermost San Andres carbonate interfingers earliest workers to document the general stratigraphic with three tongues of the Glorieta Sandstone, which is framework of the San Andres shelf and shelf-edge depos­ considered part of the San Andres Formation (Kelley, its. Other more recent outcrop studies in the Guadalupe 1971; Milner, 1974). The intertonguing San Andres/ Mountain region have concentrated on the genesis of Glorieta section was interpreted by Milner (1974) as shal­ depositional facies and correlation of shelf and basin­ low marine and tidal flat deposits, and are not included in edge strata using sequence stratigraphy and biostrati­ this study. Emphasis is placed instead on the carbonates graphic markers (Sarg and Lehmann, 1986; Hinrichs et above the uppermost tongue of the Glorieta Sandstone. al, 1986; Wilde, 1986). The only two significant outcrop studies previously made in the study area are the strati­ graphic and structural work of Kelley ( 1971) and the low­ Outcrop Stratigraphy ermost San Andres environmental study of Milner (1974, 1976). Kelley (1971) first divided the outcropping San Andres Formation of southeast New Mexico into formal mem­ bers: the lower, thicker bedded Rio Bonito Member; the GEOLO(;IC HISTORY middle, thinner bedded Bonney Canyon Member; and the upper Fourmile Draw Member (Figure 3). The Four­ The Permian basin is so-named for paleogeographic mile Draw Member is composed of thinly interbedded features that existed dunng the Permian Period. The dolomites, evaporites, and sandstones, which are poorly major tectonic events that shaped the basin began during exposed and characterized
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