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The Kootenai Formation of Western Montana records the Aptian- Albian (121.4Ma-100.5Ma), a significant interval in Earth’s history. The Early Cretaceous is notable for a multitude of changes in both the geologic and biotic realm. Significant events that occurred during this time include the tectonic evolution of the Western Interior Basin (WIB) and the displacement of gymnosperms by angiosperms. Given the significance of this time, previous and ongoing research seek to better understand the timing and interactions between these changes. The focus of this study is to refine stratigraphic constraint of the Kootenai Formation using carbon isotope chemostratigraphy. The depositional age of the lower clastic unit of the Kootenai formation has been debated over the past decade. Detrital zircon U-Pb analyses by Laskowski et al. (2013) indicated an Albian age with a U-Pb detrital zircon maximum depositional age (MDA) of 109Ma. However, more recent studies (Finezl and Rosenblume, 2020 and Rosenblume et al. 2021) using LA-ICP-MS-generated detrital zircon U-Pb analyses indicate MDAs of the lower clastic unit as old as Valanginian to Aptian (MDAs ~135-115Ma) with the upper units of the Kootenai having MDAs from Albian (~105 Ma). Detrital zircon U-Pb analyses have generally been limited in the lower units of the Kootenai particularly because syndepositionally formed zircon grains are not common in the lower units (Quin et al. 2018, Finzel and Rosenblume 2020).Additionally, previous flora in the Kootenai suggests predominately Aptian and older ages(Brown 1946). Given the limited geochronologic constraint of the lower clastic unit of the Kootenai formation, addition data is needed. For this study, approximately 60 samples from just above the basal conglomerate to the top of the lower clastic unit were collected and processed to determine bulk organic carbon isotope values. The prior MDAs suggest C isotope excursions such as those associated with OAE1a and even as old as the Valanginian Weissert event could be preserved in the strata of the lower clastic unit. The new stable isotope data will provide an opportunity to refine the age of these Cretaceous units leveraging the existing U-Pb data.
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Age of the Huolinhe Formation in the Huolinhe Basin, eastern Inner Mongolia, China: Evidence from U-Pb zircon dating and palynological assemblages
The Huolinhe Formation in the Huolinhe Basin, eastern Inner Mongolia is one of the most important Lower Cretaceous coal-bearing strata in China, yielding abundant, diverse, and well-preserved plant fossils. Its precise age, however, is poorly known due to lack of associated marine deposits and volcanic beds. Here we present U-Pb zircon ages, and the associated palynological assemblages of an ash layer of the Huolinhe Formation recently discovered at the Zhahanaoer open-cast coal mine in Jarud Banner. Stratigraphic analyses based on boreholes suggest that the ash layer occurs near the bottom of the “lower coal-bearing member” of the Huolinhe Formation. U-Pb zircon geochronology using the SIMS method constrains the depositional age of the ash layer to be 125.6 1.0 Ma (late Barremian–earliest Aptian), and this is consistent with the result from LA-ICP-MS analyses of the same sample. A late Barremian–earliest Aptian age for the ash layer is also supported by the palynological assemblage associated with the layer, in which the pollen of gymnosperms and the spores of ferns and bryophytes are dominant, angiosperm pollen is very rare and represented by only Clavatipollenites. This study contributes important new data for understanding the age of the entire Huolinhe Formation and also provides a more precise maximum age for the key plant fossils preserved in the deposits above the ash layer.
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- Award ID(s):
- 1748286
- PAR ID:
- 10316835
- Date Published:
- Journal Name:
- Dicengxue zazhi
- Volume:
- 45
- ISSN:
- 0253-4959
- Format(s):
- Medium: X
- Sponsoring Org:
- National Science Foundation
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- Free Publicly Accessible Full Text
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Accepted Manuscript1.0
- Journal Article:
- https://doi.org/10.19839/j.cnki.dcxzz.2021.0001
