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Ilew Merico Geological Socieg in a warm sea. The upper member marks a Morrowan at the widespread basal Pennsyl- return to a clastics-dominated system where a vanian unconformity and to northward trans- significant influx of silt- and clay-size material gression during Morrowan time. In spite of the acted to reduce carbonate production during Morrowan-Atokan boundary problem, the re- the final stages of Paradise deposition. While maining upper Atokan through Virgilian strata ilewMerico Geological Socieg the sources of the terrigeneous material in the make up the bulk of the section within the Paradise Formation are not well established, study area and are much better constrained The New Mexico GeologicalSociety an- the changes in the rate of sediment delivery to than the Morrowan and lower Atokan. Fusu- nual spring meeting was held at New the basin are consistent with increased tecton- linid biozones within these strata parallel the Mexico Institute of Mining and Technol- ism related to the onset of the Ouachita orog- lithoshatigraphic cydes and link sub-surfaceand ogy (Socorro)on April 16,1993.Following eny. surface stratigraphy. Findings are presented as are abstracts from sessionsgiven at that fence diagrams, isopach maps, correlation di- meeting. Abstractsfrom other sessionswill agrams, a composite Pennsylvanian type log for the study area, and a compilation of bio- appear in future issuesof NewMexico Ge- Sunsunracr srRATlcRApHy oF PENNSyLVANTAN stratigraphic data available thus far. A north- ology. of the fol- STRATABENEATN TNE JONNEOADEL MUERTO, south subsurface section consisting sourH-cENTRAL Nrw Mrxco, by A. M. West, lowing four wells, Gulf Oil Co. Sierra K State Stratigraphy, sedimentology, and T. F. Inwton, G. H. Mack, and R. E. Clemons, No. 1, Shell Oil Co. No. 1 Leeman Federal, geochronology session Department of Geological Sciences, New Exxon Corp. No. 1 Beard Federal, and Exxon Mexico State University, Las Cruces, New Corp. No. 1 Prisor Unit Federal, demonstrates Srnetrcnepny AND sEDTMENTATToNop rnE Pen- Mexico 88003 subsurface thickening and thinning trends aorsr FonvarroN (LarE within Pennsylvanian deposits. Fence dia- MrssrssrrnN) tN rnE Subsurface correlations tied to previous sur- Ppr-oNcrr-r-o grams and isopach maps linking previous sur- Moulralvs, Hroalco CouNry, face stratigraphic studies provide-an improved face work with subsurface sections show parallel Nnw Mrxco, by Daoid |. Siolls, New Mexico stratigraphic framework for the western por- Bureau of Mines strata thinning to the north and thickeniirg dra- and Mineral Resources, So- tion of the Orogrande Basin as well as the ad- corro, New Mexico matically basinward to the east. 87801 and Department of jacent northeastem portion of the Robledo shelf. Geoscience, New Mexico Institute of Mining Extensive work has been completed on out- and Technology, Socorro, New Mexico 87801; crops containing Pennsylvanian strata within and D. B. lohnson, Department of Geosci- this area located primarily within south-central ence, New Mexico Institute of Mining and New Mexico; however, previous work has done Typr Cunrrs AND SUMMERVTLLEFoRMATroNs, Technology, Socorro, New Mexico 87801 little to integrate existing surface knowledge sournresunN UrAH, by G. N. Pipiringos,U.S. The section of Paradise Formation exposed with the available surface database and pre- Geological Survey (retired), 1709 Brown Road, in the Peloncillo Mountains marks the north- viously unavailable fusulinid data. The focus Las Cruces, New Mexico 88005; and R. B. ernmost and westernmost exposure of Paradise of the presentation is an area located imme- O'Sullioan, U. S. Geological Survey, Box 25046, in New Mexico. The Paradis-eFormation is 60 diately north of Las Cruces and southeast of M!939, Federal Center, Denvet Colorado m in the central Peloncillo Mountains and is the San Mateo uplift, between the Caballo and 8022s-0046 composed of a series of yellowish-brown San Andres Mountains. The obiectives of the The Summerville Formation, San Rafael Swell, weathering, slope-forming, mixed carbonates study are to determine the subsidence and dep- Utah, is unfossiliferous but intertongues with and siliciclastics. Stratigraphically, the Paradise ositional history of the western part of the ba- and grades down into the Curtis Formation, lies conformably above t^heEscabrosa Group sin and adiacent eastern shelf as well as link which contains lithologies and fossils identical and disconformably below the Pennsylvanian previous surface stratigraphic work with sub- to those in the Pine Butte Member of the Sund- Horquilla Limestone. Although the Paradise in surface findings. A combination of well-log ance Formation of late Middle Jurassic age (Cal- the Peloncillos has undergone at least one rel- analysis, fusulinid biostratigraphy, cuttings lovian). The Pine Butte is unconformably atively mild metamorphic event, many of the descriptions, and previous geochemical anal- overlain by the Redwater Shale of Late Jurassic original depositional textures in the carbonates yses and core descriptions creates a compre- age (Oxfordian). which in turn is unconform- remain intact, allowing for some interpretation hensive subsurface database that allows ably overlain by the Windy Hill Sandstone of of depositional environrnents. In the Peloncillo correlation of strata throughout the study area. Late Jurassic age (Kimmeridgian). The Sum- Mountains the Paradise Formation can be di- Pennsylvanian strata within the Orogrande Ba- merville and the Redwater Shale are uncon- vided into several informal members: a lower sin are markedly cyclic, dominantly shallow- formably overlain by the Tidwell Member of siliciclastic-dominated member, a middle car- marine deposits of Morrowan to Virgilian age. the Morrison. The Tidwell is the southwestern bonate-dominated member, and an upper, fine- The cyclic character of the well-log response extension of the Windy Hill Sandstone. These grained siliciclastic-dominated member. The within the subsurface sections permits delin- correlations are constrained bv the presence of lower siliciclastic member consists of a single eation of upward-shoaling parasequence sets the J-2, J-3 and J-5 unconformities in the San lithofacies composed of fine-grained, rounded consisting predominantly of shale and lime- Rafael Swell and by presence of tll.e JJ, J-4 to subrounded quartz arenites. The middle car- stone packages indicating periods of trans- and f-5 unconformities in southeastern Wyo- bonate member is composed of either a grain- gression and regression within the basin. The ming and in the Black Hills. Some or all of these rich or a grain-poor lithofacies. The grain-rich log response within the middle to upper Des- unconformities have long been overlooked, lithofacies contains abundant ooids, pelmato- moinesian clearly shows a marker unit believed looked for but not found, not looked for at all, zoan fragments, and rare brachiopods. The to be an unconformity truncating the stage. misunderstood, misplaced, or misidentified, grain-poor lithofacies is composed entirely of Consistent cvclicitv within these strata results most recentlv bv Anderson and Lucas (Nezp medium-grained, equigra nul-ar sparry caliite. in confident lithoitratigraphic correlation be- Mexico Geology, iggz, u. 74, no. 4, pp. 79-92) Very fine grained to silt-size quartz is found in tween wells, except with regard to the Mor- in the San Rafael Swell and vicinity. The re- trace amounts throughout the carbonates. rowan. Presence of the Morrowan within the sulting disagreements with prior work are due Overlying the carbonate member is a series of study area is subject to debate. While the fu- to the lack of effective means of communicating interbedded carbonates and shales. The car- sulinid biozone Eoschubertella indicates early stratigraphic field data. Some caveats and sug- bonates are similar to those in the middle mem- Atokan time (Clopine, 7992; tNilde, 1990), the gestions are offered to alleviate some of the ber. For the most part any textures in the shales fusulinid biozones Millerella and Eostaffelln are differences of opinion. were obliterated during metamorphism. The diagnostic of the Morrowan. Unforiunately, lower member is interpreted as representing Lower Pennsylvanian fusulinid samples avail- deposition in a shallow, offshore, siliciclasticl able in the subsurface sections are limited. Thick dominated system as sea level gradually fell Morrowan strata are present in surface out- MoRRISoN Forur.tertoN suBDIVIstoNs,NoRTHwEST during the Late Mississippian. On a Q-F-R di- crops at Vinton Canyon (75 m thick) and Bishop Nnw Mexco: A REASsESSMENT,by Orin l. An- agram these sandstones plot exclusively on the Cap (44 m thick) located in the southwestem derson, New Mexico Bureau of Mines and Q pole indicating that these are rerycled sands portion of the basin. However, the Morrowan Mineral Resources, Socorro, New Mexico derived from a cratonic source. The middle car- thins substantially to the north (Clopine, 1992), 87807; Spencer G. Lucas, New Mexico Mu- bonate member marks a return to more stable, where it is only 1 m thick in the Derry Hills seum of Natural History and Science, 1801 clear-water carbonate conditions. The abun- section and is completelv absent in the Mud Mountain Road, NW, Albuquerque, New dant ooids and abraded grains suggest a lo- Springs section. Clirpine- (1992) attributes this Mexico 87lM; and Charles H. Maxwell, U.S. cation well within the zone of constant agitation substantial thinning to both the loss of the lower Geological Survey (retired) r= New
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