California River

Last updated January 03, 2024

California River is the name of a northeastward flowing river system that existed in the Cretaceous-Eocene in the western United States. It is so named because it flowed from the Mojave region of California to the Uinta Basin of Utah, transporting sediments along this track towards Lake Uinta.

Course

The river originated in the North American Cordillera of California^{[lower-alpha 1]}^[1] in the Mojave ^[2]/Alisitos arc,^[3] between the Nevadaplano farther north and the Mexicoplano farther south.^[2] It then flowed east-northeastward between the Sevier fold-and-thrust belt to the north and the Maria fold-and-thrust belt to the south. It continued northeastward between the Kaibab and the Circle Cliffs uplift and eventually turned due north between the Uncompahgre and San Rafael swells.^[3] The course of the river extended over 1,000 kilometres (620 mi).^[4] Ancestral Little Colorado River was a tributary, and the ancestral Mogollon Highlands also drained in this river system.^[5]

The river ended in the Uinta Basin ^[6]^{[lower-alpha 2]} and Lake Uinta in present-day Utah ^[7] roughly where the Green River exits the basin,^[8] forming a river delta that today comprises the voluminous Colton Formation ^[3] and with its sediment covering an area of over 3,000 square kilometres (1,200 sq mi).^[9] The so-called "Sunnyside Delta" has also been interpreted as a product of the California River.^[10]

In the Paleocene, this river system may have formed the headwater of river systems that ended in the Gulf of Mexico ^[11] through a paleo-Platte River ^[12] and before that it may have drained into the Arctic Ocean.^[13] A drainage through the Little Colorado River valley towards the San Juan Basin is also possible but there is no evidence,^[14] and petrological information on sediments excludes that the Piceance Creek Basin as an endpoint of California River waters.^[15]

This river system was of similar scale to the present-day Colorado River-Green River system, but with opposite direction.^[16] Analogies have been drawn between the California River and the present-day Ili River in Central Asia, both in terms of its geomorphology and the sizes and shapes of their deltas and terminal lakes.^[17]

Hydrology

The river had a high^[1] but variable discharge, which has been documented from the delta deposits.^[17]

Geological history and present-day evidence

The age of the Western Grand Canyon is controversial, with evidence both of an old Mesozoic and a young Neozoic age. In the former case,^[18] it is possible that the river created an early Grand Canyon during the Campanian ^[1] or the Paleocene.^[19]

The California River has been proposed to explain the origin of the deltaic Colton Formation, as it has a high volume and similar source rocks are rare in the area of the Uinta Basin. Rock formations of similar origin occur in southeastern California and southwestern Arizona^[4] and may have been located along the same drainage.^[20] Eroded material from the Kaiparowits Formation probably did not contribute much to the formation of the Colton Formation.^[21] The existence of the California river and whether the river that formed the deltaic Colton Formation and the early Grand Canyon were the same are subject to debate.^[22]

A similar, but more north-northeasterly drainage to the present-day Kaiparowits Plateau may have existed during the Turonian.^[23] During the Cretaceous and Paleogene, the beginning Laramide orogeny disrupted drainages in what today are the western United States, forming several closed basins where drainage ponded from as far as California.^[24] The California River existed in the Paleocene and Eocene.^[25] During the Paleocene, the collapse of the continental borderland and the Laramide orogeny reversed the course of the California River.^[1] In the Eocene, the drainage divide migrated northeastward.^[2]

Notes

↑ The California River is named after its headwaters.^[1]
↑ This is unlike drainages in the southeastern half of the Colorado Plateau which formed river deltas on the western shore of the Western Interior Seaway and the area of the Gulf of Mexico. Other rivers drained into closed basins.^[6]

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References

1 2 3 4 5 Wernicke 2009, p. 33.
1 2 3 Ingersoll et al. 2018, p. 446.
1 2 3 Davis et al. 2010, p. 931.
1 2 Davis et al. 2010, p. 932.
↑ Beard et al. 2011, p. 120.
1 2 Cather, Chapin & Kelley 2012, p. 1181.
↑ Smith, Carroll & Scott 2015, p. 72.
↑ Wang & Plink-Björklund 2019, p. 911.
↑ Foreman & Rasmussen 2016, p. 1352.
↑ Wang & Plink-Björklund 2019, p. 895.
↑ Pettit et al. 2019, p. 284.
↑ Pecha et al. 2022, p. 285.
↑ Sharman et al. 2017, p. 189.
↑ Karlstrom et al. 2017, p. 55.
↑ Foreman & Rasmussen 2016, p. 1353.
↑ Beard et al. 2011, p. 80.
1 2 Wang & Plink-Björklund 2019, p. 913.
↑ Flowers, Farley & Ketcham 2015, p. 430.
↑ Gehrels 2014, p. 138.
↑ Davis et al. 2010, p. 933.
↑ Dickinson et al. 2012, p. 869.
↑ Karlstrom et al. 2020, p. 1448.
↑ Primm, Johnson & Stearns 2018, p. 267.
↑ Foreman & Rasmussen 2016, p. 1345.
↑ Birgenheier et al. 2020, p. 584.

Sources

Beard, L.S.; Karlstrom, K.E.; Young, R.A.; Billingsley, G.H. (2011). "CRevolution 2—Origin and evolution of the Colorado River system, workshop abstracts: U.S. Geological Survey Open-File Report 2011–1210".
Birgenheier, L. P.; Berg, M. D. Vanden; Plink-Björklund, P.; Gall, R. D.; Rosencrans, E.; Rosenberg, M. J.; Toms, L. C.; Morris, J. (1 March 2020). "Climate impact on fluvial-lake system evolution, Eocene Green River Formation, Uinta Basin, Utah, USA". GSA Bulletin. 132 (3–4): 562–587. doi:10.1130/B31808.1. ISSN 0016-7606. S2CID 197586166.
Cather, Steven M.; Chapin, Charles E.; Kelley, Shari A. (1 December 2012). "Diachronous episodes of Cenozoic erosion in southwestern North America and their relationship to surface uplift, paleoclimate, paleodrainage, and paleoaltimetry". Geosphere. 8 (6): 1177–1206. doi: 10.1130/GES00801.1 .
Davis, Steven J.; Dickinson, William R.; Gehrels, George E.; Spencer, Jon E.; Lawton, Timothy F.; Carroll, Alan R. (1 October 2010). "The Paleogene California River: Evidence of Mojave-Uinta paleodrainage from U-Pb ages of detrital zircons". Geology. 38 (10): 931–934. doi:10.1130/G31250.1. ISSN 0091-7613. S2CID 129376203.
Dickinson, William R.; Lawton, Timothy F.; Pecha, Mark; Davis, Steven J.; Gehrels, George E.; Young, Richard A. (1 August 2012). "Provenance of the Paleogene Colton Formation (Uinta Basin) and Cretaceous–Paleogene provenance evolution in the Utah foreland: Evidence from U-Pb ages of detrital zircons, paleocurrent trends, and sandstone petrofacies". Geosphere. 8 (4): 854–880. doi: 10.1130/GES00763.1 .
Flowers, Rebecca M.; Farley, Kenneth A.; Ketcham, Richard A. (15 December 2015). "A reporting protocol for thermochronologic modeling illustrated with data from the Grand Canyon". Earth and Planetary Science Letters. 432: 425–435. doi: 10.1016/j.epsl.2015.09.053 . ISSN 0012-821X.
Foreman, Brady Z.; Rasmussen, Dirk M. (1 December 2016). "Provenance Signals In the Piceance Creek Basin: Unroofing of the Sawatch Range and Extent of the Early Paleogene California River System (Colorado, U.S.A.)B.Z. FOREMAN AND D.M. RASMUSSENPROVENANCE OF THE WASATCH FORMATION (PICEANCE CREEK BASIN, COLORADO, U.S.A.)". Journal of Sedimentary Research. 86 (12): 1345–1358. doi:10.2110/jsr.2016.81. ISSN 1527-1404.
Gehrels, George (30 May 2014). "Detrital Zircon U-Pb Geochronology Applied to Tectonics". Annual Review of Earth and Planetary Sciences. 42 (1): 127–149. doi: 10.1146/annurev-earth-050212-124012 .
Ingersoll, Raymond V.; Spafford, Claire D.; Jacobson, Carl E.; Grove, Marty; Howard, Jeffrey L.; Hourigan, Jeremy; Pedrick, Jane (2018), "Provenance, paleogeography, and paleotectonic implications of the mid-Cenozoic Sespe Formation, coastal southern California, USA", Tectonics, Sedimentary Basins, and Provenance: A Celebration of the Career of William R. Dickinson, Geological Society of America, doi:10.1130/2018.2540(20), ISBN 978-0-8137-2540-6 , retrieved 2020-10-05
Karlstrom, K. E.; Crossey, L. J.; Embid, E.; Crow, R.; Heizler, M.; Hereford, R.; Beard, L. S.; Ricketts, J. W.; Cather, S.; Kelley, S. (1 February 2017). "Cenozoic incision history of the Little Colorado River: Its role in carving Grand Canyon and onset of rapid incision in the past ca. 2 Ma in the Colorado River System". Geosphere. 13 (1): 49–81. doi: 10.1130/GES01304.1 .
Karlstrom, Karl E.; Jacobson, Carl E.; Sundell, Kurt E.; Eyster, Athena; Blakey, Ron; Ingersoll, Raymond V.; Mulder, Jacob A.; Young, Richard A.; Beard, L. Sue; Holland, Mark E.; Shuster, David L.; Winn, Carmen; Crossey, Laura (1 December 2020). "Evaluating the Shinumo-Sespe drainage connection: Arguments against the "old" (70–17 Ma) Grand Canyon models for Colorado Plateau drainage evolution". Geosphere. 16 (6): 1425–1456. doi: 10.1130/GES02265.1 . hdl: 2440/135048 .
Pecha, Mark E.; Blum, Michael D.; Gehrels, George E.; Sundell, Kurt E.; Karlstrom, Karl E.; Gonzales, David A.; Malone, David H.; Mahoney, J. Brian (2022-05-03), Craddock, John P.; Malone, David H.; Foreman, Brady Z.; Konstantinou, Alexandros (eds.), "Linking the Gulf of Mexico and Coast Mountains batholith during late Paleocene time: Insights from Hf isotopes in detrital zircons", Tectonic Evolution of the Sevier-Laramide Hinterland, Thrust Belt, and Foreland, and Postorogenic Slab Rollback (180–20 Ma), Geological Society of America, pp. 265–292, doi:10.1130/2021.2555(10), ISBN 978-0-8137-2555-0 , retrieved 2023-04-05– via ResearchGate
Pettit, Bridget S.; Blum, Mike; Pecha, Mark; McLean, Noah; Bartschi, Nicolas C.; Saylor, Joel E. (11 April 2019). "Detrital-Zircon U-Pb Paleodrainage Reconstruction and Geochronology of the Campanian Blackhawk–Castlegate Succession, Wasatch Plateau and Book Cliffs, Utah, U.S.A." Journal of Sedimentary Research. 89 (4): 273–292. doi:10.2110/jsr.2019.18. ISSN 1527-1404. S2CID 146547554.
Primm, Jonathan W.; Johnson, Cari L.; Stearns, Michael (April 2018). "Basin-axial progradation of a sediment supply driven distributive fluvial system in the Late Cretaceous southern Utah foreland". Basin Research. 30 (2): 249–278. doi:10.1111/bre.12252. S2CID 133822007.
Sharman, Glenn R.; Covault, Jacob A.; Stockli, Daniel F.; Wroblewski, Anton F.-J.; Bush, Meredith A. (1 February 2017). "Early Cenozoic drainage reorganization of the United States Western Interior–Gulf of Mexico sediment routing system". Geology. 45 (2): 187–190. doi:10.1130/G38765.1. ISSN 0091-7613.
Smith, Michael Elliot; Carroll, Alan R.; Scott, Jennifer Jane (2015), Smith, Michael Elliot; Carroll, Alan R. (eds.), "Stratigraphic Expression of Climate, Tectonism, and Geomorphic Forcing in an Underfilled Lake Basin: Wilkins Peak Member of the Green River Formation", Stratigraphy and Paleolimnology of the Green River Formation, Western USA, Syntheses in Limnogeology, Dordrecht: Springer Netherlands, vol. 1, pp. 61–102, doi:10.1007/978-94-017-9906-5_4, ISBN 978-94-017-9905-8 , retrieved 2020-10-04
Wang, Jianqiao; Plink-Björklund, Piret (October 2019). "Stratigraphic complexity in fluvial fans: Lower Eocene Green River Formation, Uinta Basin, USA". Basin Research. 31 (5): 892–919. doi:10.1111/bre.12350. S2CID 135391382.
Wernicke, B. (2009). The California River and its role in carving Grand Canyon. Geological Society of America Abstracts with Programs. Vol. 41. p. 33.

External links

Jones, Evan Rhys (2017). Probabilistic source-to-sink analysis of the provenance of the California paleoriver : implications for the early Eocene paleogeography of western North America (Thesis thesis). Colorado School of Mines. Arthur Lakes Library.

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[2] The California River is named after its headwaters.^[1]

[8] This is unlike drainages in the southeastern half of the Colorado Plateau which formed river deltas on the western shore of the Western Interior Seaway and the area of the Gulf of Mexico. Other rivers drained into closed basins.^[6]

[FOOTNOTEWernicke200933-1] 1 2 3 4 5 Wernicke 2009, p. 33.

[FOOTNOTEIngersollSpaffordJacobsonGrove2018446-3] 1 2 3 Ingersoll et al. 2018, p. 446.

[FOOTNOTEDavisDickinsonGehrelsSpencer2010931-4] 1 2 3 Davis et al. 2010, p. 931.

[FOOTNOTEDavisDickinsonGehrelsSpencer2010932-5] 1 2 Davis et al. 2010, p. 932.

[FOOTNOTEBeardKarlstromYoungBillingsley2011120-6] Beard et al. 2011, p. 120.

[FOOTNOTECatherChapinKelley20121181-7] 1 2 Cather, Chapin & Kelley 2012, p. 1181.

[FOOTNOTESmithCarrollScott201572-9] Smith, Carroll & Scott 2015, p. 72.

[FOOTNOTEWangPlink-Björklund2019911-10] Wang & Plink-Björklund 2019, p. 911.

[FOOTNOTEForemanRasmussen20161352-11] Foreman & Rasmussen 2016, p. 1352.

[FOOTNOTEWangPlink-Björklund2019895-12] Wang & Plink-Björklund 2019, p. 895.

[FOOTNOTEPettitBlumPechaMcLean2019284-13] Pettit et al. 2019, p. 284.

[FOOTNOTEPechaBlumGehrelsSundell2022285-14] Pecha et al. 2022, p. 285.

[FOOTNOTESharmanCovaultStockliWroblewski2017189-15] Sharman et al. 2017, p. 189.

[FOOTNOTEKarlstromCrosseyEmbidCrow201755-16] Karlstrom et al. 2017, p. 55.

[FOOTNOTEForemanRasmussen20161353-17] Foreman & Rasmussen 2016, p. 1353.

[FOOTNOTEBeardKarlstromYoungBillingsley201180-18] Beard et al. 2011, p. 80.

[FOOTNOTEWangPlink-Björklund2019913-19] 1 2 Wang & Plink-Björklund 2019, p. 913.

[FOOTNOTEFlowersFarleyKetcham2015430-20] Flowers, Farley & Ketcham 2015, p. 430.

[FOOTNOTEGehrels2014138-21] Gehrels 2014, p. 138.

[FOOTNOTEDavisDickinsonGehrelsSpencer2010933-22] Davis et al. 2010, p. 933.

[FOOTNOTEDickinsonLawtonPechaDavis2012869-23] Dickinson et al. 2012, p. 869.

[FOOTNOTEKarlstromJacobsonSundellEyster20201448-24] Karlstrom et al. 2020, p. 1448.

[FOOTNOTEPrimmJohnsonStearns2018267-25] Primm, Johnson & Stearns 2018, p. 267.

[FOOTNOTEForemanRasmussen20161345-26] Foreman & Rasmussen 2016, p. 1345.

[FOOTNOTEBirgenheierBergPlink-BjörklundGall2020584-27] Birgenheier et al. 2020, p. 584.

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