Organ Rock Formation

The Organ Rock Formation or Organ Rock Shale is a formation within the late Pennsylvanian to early Permian Cutler Group and is deposited across southeastern Utah, northwestern New Mexico, and northeastern Arizona. This formation notably outcrops around Canyonlands National Park, Natural Bridges National Monument, and Monument Valley of northeast Arizona, southern Utah. The age of the Organ Rock is constrained to the latter half of the Cisuralian epoch by age dates from overlying and underlying formations. Important early terrestrial vertebrate fossils have been recovered from this formation in northern Arizona, southern Utah, and northern New Mexico. These include the iconic Permian terrestrial fauna: Seymouria, Diadectes, Ophiacodon, and Dimetrodon. The fossil assemblage present suggests arid environmental conditions. This is corroborated with paleoclimate data indicative of global drying throughout the early Permian.

Organ Rock Formation
Stratigraphic range: Early to Middle Permian:
Towers of red Organ Rock capped with White Rim Sandstone in Shafer Canyon in Canyonlands National Park
TypeGeological formation
Unit ofCutler Formation
UnderliesDe Chelly Sandstone
OverliesCedar Mesa Sandstone
Lithology
Primarysandstones, siltstones, conglomerates, and mudstones.[1]
Location
Coordinates37.124°N 110.378°W / 37.124; -110.378
RegionColorado Plateau
Extent Utah
 Colorado
 Arizona
 New Mexico
Organ Rock Formation is located in the United States
Organ Rock Formation
Organ Rock Formation (the United States)
Organ Rock Formation is located in Utah
Organ Rock Formation
Organ Rock Formation (Utah)

Geographic extent

The Organ Rock Formation is present across southeastern Utah, U.S.A. It outcrops around Canyonlands National Park, Natural Bridges National Monument, and Monument Valley.[1] In these areas the Organ Rock typically outcrops as a dark-red/brown siltstone to mudstone gently dipping towards the southeast. Within Canyonlands N.P. it forms towers which are meters to tens of meters tall. These are protected by caps of the White Rim Sandstone. In general, the Organ Rock Formation records the evolution of terminal fluvial fans, which dry up into sections of overlying formations.[2] Animals living during the time of the Organ Rock's deposition had the capacity to travel across most of earth's landmass, as at the time, land was all concentrated into the supercontinent Pangea.

Stratigraphy and age

The Organ Rock Formation is conformably underlain by the Cedar Mesa Sandstone.[3][1] It is conformably overlain by the De Chelly Sandstone around Monument Valley and by the White Rim Sandstone in the Canyonlands National Park. In locations where the De Chelly and White Rim are absent, the Organ Rock is unconformably overlain by the Triassic Moenkopi or Chinle Formations by an erosional contact. Toward its eastern extent, the Organ Rock Formation grades into the Cutler Formation, undivided. This transition occurs to the southwest of Moab, UT. The age of the Organ Rock Formation is unconfirmed.[4] The preceding Cedar Mesa Sandstone is dated to the Wolfcampian (ICS stage: Artinskian).[5] The anteceding De Chelly and White Rim Sandstones are dated to the Leonardian (ICS stage: Kungurian).[6][7] These formations constrain the age of the Organ Rock Formation to the latter part of the Cisuralian Epoch, approximately 290.1 to 272.3 Ma. The Organ Rock Formation may contain the Artinskian/Kungurian boundary. This is during the early to mid-Permian, a time where synapsids and temnospondyl amphibians are the dominant players in terrestrial ecosystems. These animals predate the advent of archosaur reptiles which give rise to dinosaurs in the Triassic.

Depositional environments

The Organ Rock Formation is composed of sandstones, siltstones, conglomerates, and mudstones.[1] These rocks occur in two primary facies: floodplain and channel, as well as eolian dunes and sand sheets.

Floodplain and channel

In these deposits, mixed reddish-brown sands and silts dominate with minor mudstones and conglomerates interspersed.[1] Interpreted channel deposits grade from laterally accreting coarse sands – into conglomerates of pebble-sized carbonate clasts. Channels are 0.5 meter to 7 meters thick and may extend laterally for a few hundred meters. Fine-grained silt to mudstone deposits are proximal to interpreted channels. These deposits are interpreted as meandering streams with associated floodplains.

Eolian dune and sand sheet

Deposits are characterized by pale red fine- to medium-grained sandstones.[1] These units are cross-bedded. Each cross-bed is composed of thin, consistently spaced laminations. These strata are interpreted as those made by migrating dunes. This facies is marked by a sharp contact at the top of the preceding floodplain and channel facies. Mud cracks found at the top of the facies are filled by fine-grained sand from the overlying dune facies. This facies is most common at the western extent of the Organ Rock Formation.

Plant fossils

Plant fossils include Supaia, Walchi and Yakia which lived in semi-arid conditions.

Vertebrate fossils

Fossil vertebrates represent the majority of the faunal assemblage present in the Organ Rock Formation.[8][9][10][11][12] Animal remains are most commonly preserved within ancient stream channels of the floodplain and channel facies. Within this facies, fossilized bone occurs proximal to conglomeratic lenses. Taxa recovered include: freshwater actinopterygian fishes, temnospondyl amphibians, diadectomorphs, seymouriamorphs, and early synapsids.

Freshwater Actinopterygian fishes

Fossil fish material, either bone or scale, is infrequent within the Organ Rock Formation.[8] Scales from the extinct group of fishes Palaeoniscoidea are present. These scales, however, are only found preserved in fossilized feces (coprolites). Some coprolites are interpreted to be from fish; others from indeterminate terrestrial vertebrates.

Temnospondyls

Temnospondyl amphibian remains are present within the Organ Rock Formation.[8] Three taxa have been reported. These include: Trimerorhachis, Eryops, and Zatrachys. Of these three taxa, fragments of Eryops are the most commonly recovered. Remains of this animal are very common in other formations of the Cutler Group and in general during the Early Permian of southwestern North America.

Diadectomorphs

Diadectomorphs are medium to large (2–3 meters), heavily-built reptiliomorphs with robust limbs. These animals are thought to be the closest outgroup to the clade Amniota. Two taxa are present within the Organ Rock Formation: Diadectes, and Tseajaia campi. Diadectes is more abundant in the Organ Rock than the other formations of the Cutler Group. Fragments of the animal are most commonly reported. The most complete two specimens include pectoral girdles and limbs. These were collected in San Juan County, Utah. Diadectes is an important animal as it is the first terrestrial vertebrate to demonstrate characteristics necessary for obligatory herbivory. These include: peg-shaped teeth in the front of the mouth, as well as broad blunt teeth used to more effectively process vegetation. Tseajaia campi is a very rare taxon known from one nearly complete specimen recovered from the Organ Rock. Originally described by Vaughn,[8] this animal was first assigned to the group Seymouriamorpha, however, upon reassessment of the holotype it was demonstrated to have a closer affinity to Diadectomorpha.[13]

Seymouriamorphs

Seymouriamorphs are small- to medium- sized (0.5 to 1.5 meters), reptiliomorphs. These animals have a generalized early amphibian body plan with a large “u”-shaped head and a sprawling lizard-like posture. The taxon Seymouria sanjuanensis is the only seymouriamorph found in the Organ Rock Formation. Seymouria sanjuanensis is a unique taxon because of its extensive geographic range. This particular animal was first described by Vaughn (1966)[9] from the Organ Rock Formation. Since this initial find, a number of these individuals have been recovered from localities as distant as Germany.[14]

Early Synapsids

Four early synapsid taxa are present within the Organ Rock Formation. These include Ophiacodon, as well as three sphenacodontids: Ctenospondylus, Dimetrodon, and Sphenacodon ferocior.[12] Most taxa are known from fragmentary material. Early synapsids were dominant members of the terrestrial Permian ecosystem.[14] Some early synapsids adapted an herbivorous diet, however, the Organ Rock Formation only preserves carnivorous animals; these were likely the apex predators of this ecosystem. The three sphenacodontids were terrestrial predators consuming other tetrapods, while Ophiacodon likely hunted fishes and other aquatic animals.

Coprolites

Coprolites associated with a labyrinthodont tooth as well as “Pelycosaur” and didectid remains have been recovered from this formation.

Paleoecological significance

The vertebrate faunal assemblage found in the Organ Rock Formation is diverse with respect to taxonomic groups, body plans, and diets. This material represents a decent cross-section of what terrestrial vertebrate life was like during the early Permian. It is noteworthy that no diapsid material has been definitively recovered from this formation.[12] As one moves younger in time through the Organ Rock Formation, temnospondyls become less abundant with respect to other major groups such as diadectomorphs and early synapsids.[8] This could track the general trend of aridification as indicated by sedimentology of the formation. This trend is globally recognized during the Early Permian, supported by many lines of geologic evidence including significant deposits of calcretes, eolianites, and evaporites.[15]

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References
  1. Stanesco, J.D.; Dubiel, R.F.; Huntoon, J.E. (2000). "Depositional Environments and Paleotectonics of the Organ Rock Formation of the Permian Cutler Group, Southeastern Utah". Utah Geological Association Publication. 28: 1–15.
  2. Cain, S.A.; Mountney, N.P. (2009). "Spatial and temporal evolution of a terminal fluvial fan system: the Permian Organ Rock Formation, South‐east Utah, USA". Sedimentology. 56 (6).
  3. Condon, S.M. (1997). "Geology of the Pennsylvanian and Permian Cutler Group and Permian Kaibab Limestone in the Paradox Basin, Southeastern Utah and Southwestern Colorado". U.S. Geological Survey Bulletin. 2000: 1–46.
  4. Baars, D.L. (1962). "Permian System of Colorado Plateau". American Association of Petroleum Geologists Bulletin. 46 (2): 1–46.
  5. Stanesco, J.D.; Campbell, J.A. (1989). "Eolian and noneolian facies of the Lower Permian Cedar Mesa Sandstone Member of the Cutler Formation, southeastern Utah". U.S. Geological Survey Bulletin. 1808 (2): F1-F13.
  6. Blakey, R.C. (1974). "Stratigraphic and depositional analysis of the Moenkopi Formation, southeastern Utah". Utah Geological and Mineral Survey Bulletin. 104: 81.
  7. Blakey, R.C. (1990). "Stratigraphy and geologic history of Pennsylvanian and Permian rocks, Mogollon Rim region, central Arizona and vicinity". Geological Society of America Bulletin. 102 (9): 1189–1217. doi:10.1130/0016-7606(1990)102<1189:saghop>2.3.co;2.
  8. Vaughn, P.P. (1964). "Vertebrates from the Organ Rock Shale of the Cutler Group, Permian of Monument Valley and Vicinity, Utah and Arizona". Journal of Paleontology. 38 (3): 567–583.
  9. Vaughn, P.P. (1966). "Comparison of the early Permian vertebrate faunas of the Four Corners region and North Central Texas". Los Angeles County Museum Contributions in Science. 105: 1–13.
  10. Vaughn, Peter P., 1973, Vertebrates from the Cutler Group of Monument Valley and vicinity in Monument Valley (Arizona, Utah and New Mexico), James, H.L.: New Mexico Geological Society 24th Annual Fall field Guidebook, 232 p.
  11. Sumida, Stuart S., Walliser, James B.D., and Lombard, B. Eric, 1999a, Late Paleozoic amphibian-grade tetrapods of Utah: Miscellaneous Publication- Utah Geological Survey, v. 99(1), p. 21 – 30.
  12. Sumida, Stuart S., Lombard, B. Eric, Berman, David S., Henrici, Amy C., 1999b, Late Paleozoic amniotes and their near relatives from Utah and northeastern Arizona, with comments on the Permian – Pennsylvanian boundary in Utah and northern Arizona: Miscellaneous Publication- Utah Geological Survey, v. 99(1), p. 21 – 30.
  13. Sumida, Stuart S., Lombard, R. E., and Berman, D. S, 1992, Morphology of the atlas axis complex of the late Palaeozoic tetrapod suborders Diadectomorpha and Seymouriamorpha: Philosophical Transactions of the Royal Society of London, v. 336, p. 259-273.
  14. Benton, Michael J., 2015, Vertebrate Palaeontology: Wiley-Blackwell, Oxford, 4th edition.
  15. Tabor, Neil J., and Poulsen, Christopher J., 2008, Palaeoclimate across the Late Pennsylvanian _ early Permian tropical palaeolatitudes: A review of climate indicators, their distribution, and relation to palaeophysiographic climate factors: Palaeogeography, Palaeoclimatology, Palaeoecology, 268, p. 293 – 310.
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