Tropic Shale

The Tropic Shale is predominantly marine mudstone and claystone, with several radioisotopically-dated bentonite marker beds and occasional sandstone layers, deposited during the late Cretaceous Period, during the Upper Cenomanian through the Middle Turonian (95-92 Ma). It has an average thickness range from 183–274 m. The Tropic Shale conformity overlies the Dakota Formation and underlies the Straight Cliffs Formation. The top of the Dakota Formation is known for its sandier coarsening up sequences and estuarine shell beds. The distinction between the Tropic Shale and underlying Dakota is marked by the appearance of marine mudstones. In some localities, there is a sharp non conformable contact between the Dakota Formation and Tropic Shale. The contact with the overlying Straight Cliffs is gradational with the distinction between the two units defined as the point where sandstone becomes more abundant than shale. The Tropic Shale has two dominant lithologies, with the lower two thirds of the formation consisting of a bluish gray calcareous mudstone that encompasses eleven ammonoid biozones. The upper third is a darker gray and non-calcareous, and encompasses only one or two ammonoid biozones. Additionally, the upper portion, hummocky cross stratified and turbiditic sandstone beds become more common. ==Stratigraphy and age==

The Tropic Shale has been correlated temporally with the Tununk Member of the Mancos Shale in central Utah, the Allen Valley Shale of the western Wasatch Range in Utah, the Mancos Shale exposed at Black Mesa, Arizona, and additionally the Bridge Creek Member of the Greenhorn Limestone at Pueblo, Colorado. Bentonite layers present in all these formations have been correlated throughout deposits associated with the Western Interior Seaway. Solid and septarian carbonate concretionary nodule horizons are characteristic of the lower and middle parts of the formation informally named as concretionary layer 1-4. The stratigraphically lowest is layer one with the stratigraphically highest being layer 4. Layers 1 and 2 seem to be in isolated sections while layers 3 and 4 seem to have a wide distribution and act as marker beds between Bentonite "A" and "B". The ammonites Sciponoceras gracile and Euomphaloceras septemseriatum are commonly preserved in these concretionary nodules. The bentonites of the Tropic Shale form erosional benches that can be easily traced throughout the formation. These bentonites have been correlated with other formations that are interpreted as part of the Western Interior Seaway. They are white to light grey when freshly exposed or can have a yellowish discoloration when weathered. The average thickness of these bentonite beds is 1–6 mm. They are organized using a lettered system (A-E) with the lowest stratigraphically positioned bentonite being "A" and the highest stratigraphically positioned bentonite being "E". Several of these bentonites have also been related to known ammonoid biozones. Bentonites "A" and "B" are associated with massive accumulations of clam fossils. Radioisotopically dated beds: ==Paleontology==

Fossils have been found throughout the entire section of the Tropic Shale. Invertebrates such as ammonites and innoceramid clams seem to dominate. Shark remains consist almost entirely of tooth remains while marine reptiles vary in preservation from isolated fragments to articulated specimens. The Tropic Shale is known for a wide assortment of marine vertebrates with minor contributions from terrestrial vertebrates. Recovered fossils include sharks, fishes, marine reptiles, turtles and dinosaurs. The marine deposition of vertebrates such as dinosaurs is interpreted as animals being washed out to sea while still alive in a storm event that then drowned or decomposing animals that were washed out to sea in a bloat and float model of transportation. Reptiles Dinosaurs Mosasaurs Plesiosaurs Turtles Fish Bony fish Cartilaginous fish Invertebrates The Tropic Shale is known for its large invertebrate assemblage. Ammonites seem to be major contributors to the ecosystem with oysters and gastropods rounding out the ecosystem. Cold hydrocarbon seeps seem to have their own invertebrate biozone located at the bottom of the formation. Rudists and solitary corals seem to be quite rare and have not been studied due to their lack of presence in the Tropic Shale as they are recorded from other formations associated with the Western Interior Seaway. Paleobotany Limited occurrences of petrified wood have been reported in the Tropic Shale. These are interpreted predominately as drift wood that settled to the bottom of the inland seaway. ==Paleoecology==

During the late Cretaceous, the Western Interior Seaway was occupied by a sea that was regressing by the Turonian. There was a brief transgression, as the estuary like Dakota Formation was replaced by deeper marine shelf deposits. This transgression/regression (named the Greenhorn) cycle lasted about four million years and correlates to an oceanic anoxic event. Evidence of the change is characterized by massive deposits of calcium carbonate in the marine mudstones that can be seen in the upper third of the Tropic Shale when calcium carbonate is absent. During the late Cretaceous, widespread conditions of oceanic anoxia occurred across the Cenomanian–Turonian (C-T) stage boundary between about 94.2 and 93.5 million years ago (Oceanic Anoxic Event II, OAE II). Cold hydrocarbon seep bioherms in the lower portion of the Tropic Shale during the Cenomanian give glimpses of different ecosystems to the marine shelf deposits. These bioherms tend to be around one meter tall and up to three meters wide with large concentrations of invertebrates surrounding the seeps. ==References==