Geology of the Rocky Mountains

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Location of the Rocky Mountains in western North America RockyMountainsLocatorMap.png
Location of the Rocky Mountains in western North America

The geology of the Rocky Mountains is that of a discontinuous series of mountain ranges with distinct geological origins. Collectively these make up the Rocky Mountains, a mountain system that stretches from Northern British Columbia through central New Mexico and which is part of the great mountain system known as the North American Cordillera.

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The rocky cores of the mountain ranges are, in most places, formed of pieces of continental crust that are over one billion years old. In the south, an older mountain range was formed 300 million years ago, then eroded away. The rocks of that older range were reformed into the Rocky Mountains.

The Rocky Mountains took shape during an intense period of plate tectonic activity that resulted in much of the rugged landscape of western North America. The Laramide orogeny, about 80–55 million years ago, was the last of the three episodes and was responsible for raising the Rocky Mountains. [1] Subsequent erosion by glaciers has produced the current form of the mountains.

Precambrian

Precambrian cratons and orogens in the Rocky Mountain area Wyoming, Mojave, Yavapai, Mazatzal, Trans-Hudson.gif
Precambrian cratons and orogens in the Rocky Mountain area

The rocks in the Rocky Mountains were formed before the mountains were raised by tectonic forces. The oldest rock is Precambrian Wyoming craton that forms the core of the North American continent. The Wyoming Craton originated as a 100,000 km2 middle Archean craton that was modified by late Archean volcanic magmatism and plate movements and Proterozoic extension and rifting. [2] The Wyoming Craton mainly consists of two rock units: granitoid plutons (2.8–2.55 Ga) and gneiss and migmatite. The granitoid rocks are mainly potassic granite and were derived principally from reworked older (3.1–2.8 Ga) gneiss. [3]

During the Paleoproterozoic, island-arc terrane associated with the Colorado orogeny accreted to the Wyoming Craton along the Cheyenne belt, a 500-km-wide belt of Proterozoic rocks named for Cheyenne, Wyoming. As a result of the collision, older, Archean rocks of the Wyoming craton were intensely deformed and metamorphosed for at least 75 km inboard from the suture, which is marked today by the Laramie Mountains. [3] The Colorado orogeny was likely part of the larger Yavapai orogeny, which extended across North America and probably to other continents that were joined to North America as part of the supercontinent, Columbia. [4]

In the Paleoproterozoic, terranes also accumulated on the west side of the Wyoming Craton, forming the Selway terrane in Idaho. [5]

Mesoproterozoic (~1.4 Ga) anorthosite and syenites of the Laramie Anorthosite Complex and granite intrude into rocks of the Colorado orogen in the Laramie and adjacent Medicine Bow Mountains. Both the anorthosite and granite transect the Cheyenne belt in the Laramide Mountains, and intrude crystalline rocks of the Wyoming province. These intrusions comprise the northernmost segment of a wide belt of 1.4 Ga granitic intrusions that occur throughout the Colorado orogen. [3]

The breakup of the Rodinia supercontinent produced rifts between 900 million and 600 million years ago in the Neoproterozoic. These deep extensional basement faults filled with sediments, such as the Uinta rift basin and were reactivated more recently in Earth history by orogenies. The Uinta Formation and Uncompahgre Formation are both examples of remnant Precambrian rift basin sediments.[ citation needed ] The end of the Neoproterozoic is not known from the rock record, indicating a period of long-running terrestrial erosion which produced by the Great Unconformity, from 1.1 billion to 510 million years ago. Twelve to 24 kilometers of basement rock eroded away. [6]

Ancestral Rocky Mountains

During the Paleozoic, western North America lay underneath a shallow sea, which deposited many kilometers of limestone and dolomite. [7]

In the southern Rocky Mountains, near present-day Colorado and New Mexico, the Precambrian and Paleozoic rocks were disturbed by mountain building approximately 300 Ma, during the Pennsylvanian. This mountain building produced the Ancestral Rocky Mountains. [8] : 1  The uplift formed two large mountainous islands, known to geologists as Frontrangia and Uncompahgria, located roughly in the current locations of the Front Range and the San Juan Mountains. They consisted largely of Precambrian metamorphic rock, forced upward through layers of the limestone laid down in the shallow sea. [9] The mountains eroded throughout the late Paleozoic and early Mesozoic, leaving extensive deposits of sedimentary rock. [8] : 6 

Western Interior Seaway 95 million years ago Western Interior Seaway - 95Ma.svg
Western Interior Seaway 95 million years ago

Mesozoic deposition in the Rockies occurred in a mix of marine, transitional, and continental environments as local relative sea levels changed. By the close of the Mesozoic, 10,000 to 15,000 feet (3000 to 4500 m) of sediment accumulated in 15 recognized formations. The most extensive non-marine formations were deposited in the Cretaceous period when the western part of the Western Interior Seaway covered the region. [10]

Mesozoic terranes and subduction

Terranes started to collide with the western edge of North America in the Mississippian age (approximately 350 million years ago), causing the Antler orogeny. [11] During the last half of the Mesozoic Era, much of today's California, British Columbia, Oregon, and Washington were added to North America. Western North America suffered the effects of repeated collision as the Kula and Farallon Plates sank beneath the continental edge. Slivers of continental crust, carried along by subducting ocean plates, were swept into the subduction zone and scraped onto North America's western edge. [12]

These terranes represent a variety of tectonic environments. Some are ancient island arcs, similar to Japan, Indonesia and the Aleutians; others are fragments of oceanic crust obducted onto the continental margin while others represent small isolated mid-oceanic islands. [13]

Sketch of an oceanic plate subducting beneath a continental plate at a collisional plate boundary. The oceanic plate typically sinks at a high angle (exaggerated here). A volcanic arc grows above the subducting plate. Active Margin.svg
Sketch of an oceanic plate subducting beneath a continental plate at a collisional plate boundary. The oceanic plate typically sinks at a high angle (exaggerated here). A volcanic arc grows above the subducting plate.

Magma generated above the subducting slab rose into the North American continental crust about 200 to 300 miles (300 to 500 km) inland. Great arc-shaped volcanic mountain ranges, known as the Sierran Arc, grew as lava and ash spewed out of dozens of individual volcanoes. Beneath the surface, great masses of molten rock were injected and hardened in place. [12]

For 270 million years, the effects of plate collisions were focused very near the edge of the North American Plate boundary, far to the west of the Rocky Mountain region. [11] It was not until 80 MA that these effects began to reach the Rockies. [1]

Raising the Rockies

The current Rocky Mountains were raised in the Laramide orogeny from between 80 and 55 Ma. [1] For the Canadian Rockies, the mountain building is analogous to a rug being pushed on a hardwood floor: [14] : 78  the rug bunches up and forms wrinkles (mountains). In Canada, the subduction of the Kula plate and the terranes smashing into the continent are the feet pushing the rug, the ancestral rocks are the rug, and the Canadian Shield in the middle of the continent is the hardwood floor. [14] : 78 

Farther south, the growth of the Rocky Mountains in the United States is a geological puzzle. [1] Mountain building is normally focused between 200 and 400 miles (300 and 600 km) inland from a subduction zone boundary. Geologists continue to gather evidence to explain the rise of the Rockies so much farther inland; the answer most likely lies with the unusual subduction of the Farallon plate, [12] or possibly due to the subduction of an oceanic plateau. [1] [15]

At a typical subduction zone, an oceanic plate typically sinks at a fairly steep angle, and a volcanic arc grows above the subducting plate. During the growth of the Rocky Mountains, the angle of the subducting plate may have been significantly flattened, moving the focus of melting and mountain building much farther inland than is normally expected. [12] It is postulated that the shallow angle of the subducting plate greatly increased the friction and other interactions with the thick continental mass above it. Tremendous thrusts piled sheets of crust on top of each other, building the extraordinarily broad, high Rocky Mountain range. [12]

Tilted slabs of sedimentary rock in Colorado Roxborough.jpg
Tilted slabs of sedimentary rock in Colorado

The current southern Rockies were forced upwards through the layers of Pennsylvanian and Permian sedimentary remnants of the Ancestral Rocky Mountains. Such sedimentary remnants were often tilted at steep angles along the flanks of the modern range; they are now visible in many places throughout the Rockies, and are prominently shown along the Dakota Hogback, an early Cretaceous sandstone formation that runs along the eastern flank of the modern Rockies.

Current landscape

Immediately after the Laramide orogeny, the Rockies were like Tibet: a high plateau, probably 6,000 metres (20,000 ft) above sea level. In the last 60 million years, erosion stripped away the high rocks, revealing the ancestral rocks beneath, and forming the current landscape of the Rockies. [14] : 80–81 

Glaciers, such as Jackson Glacier as shown here, have dramatically shaped the Rocky Mountains. Jackson Glacier terminus.jpg
Glaciers, such as Jackson Glacier as shown here, have dramatically shaped the Rocky Mountains.

Multiple periods of glaciation occurred during the Pleistocene Epoch (1.8 million–12,000 years ago), finally receding in the Holocene Epoch (fewer than 11,000 years ago). The ice ages left their mark on the Rockies, forming extensive glacial landforms, such as U-shaped valleys and cirques. Recent glacial episodes included the Bull Lake Glaciation that began about 150,000 years ago and the Pinedale Glaciation that probably remained at full glaciation until 15,000–20,000 years ago. [16] [17] Ninety percent of Yellowstone National Park was covered by ice during the Pinedale Glaciation. [16] The little ice age was a period of glacial advance that lasted a few centuries from about 1550 to 1860. For example, the Agassiz and Jackson Glaciers in Glacier National Park reached their most forward positions about 1860 during the Little Ice Age. [16]

All of the geological processes, above, have left a complex set of rocks exposed at the surface. For example, in the Rockies of Colorado, there is extensive granite and gneiss dating back to the Ancestral Rockies. In the central Canadian Rockies, the main ranges are composed of the Precambrian mudstones, while the front ranges are composed of the Paleozoic limestones and dolomites. [18] Volcanic rock from the Cenozoic (66 million–1.8 million years ago) occurs in the San Juan Mountains and in other areas. Millennia of severe erosion in the Wyoming Basin transformed intermountain basins into a relatively flat terrain. The Tetons and other north-central ranges contain folded and faulted rocks of Paleozoic and Mesozoic age draped above cores of Proterozoic and Archean igneous and metamorphic rocks ranging in age from 1.2 billion (e.g., Tetons) to more than 3.3 billion years (Beartooth Mountains). [16]

See also

Related Research Articles

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<span class="mw-page-title-main">Laramide orogeny</span> Period of mountain building in North America

The Laramide orogeny was a time period of mountain building in western North America, which started in the Late Cretaceous, 80 to 70 million years ago, and ended 55 to 35 million years ago. The exact duration and ages of beginning and end of the orogeny are in dispute. The Laramide orogeny occurred in a series of pulses, with quiescent phases intervening. The major feature that was created by this orogeny was deep-seated, thick-skinned deformation, with evidence of this orogeny found from Canada to northern Mexico, with the easternmost extent of the mountain-building represented by the Black Hills of South Dakota. The phenomenon is named for the Laramie Mountains of eastern Wyoming. The Laramide orogeny is sometimes confused with the Sevier orogeny, which partially overlapped in time and space.

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<span class="mw-page-title-main">Laurentia</span> Craton forming the geological core of North America

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<span class="mw-page-title-main">Geology of Arizona</span>

The geology of Arizona began to form in the Precambrian. Igneous and metamorphic crystalline basement rock may have been much older, but was overwritten during the Yavapai and Mazatzal orogenies in the Proterozoic. The Grenville orogeny to the east caused Arizona to fill with sediments, shedding into a shallow sea. Limestone formed in the sea was metamorphosed by mafic intrusions. The Great Unconformity is a famous gap in the stratigraphic record, as Arizona experienced 900 million years of terrestrial conditions, except in isolated basins. The region oscillated between terrestrial and shallow ocean conditions during the Paleozoic as multi-cellular life became common and three major orogenies to the east shed sediments before North America became part of the supercontinent Pangaea. The breakup of Pangaea was accompanied by the subduction of the Farallon Plate, which drove volcanism during the Nevadan orogeny and the Sevier orogeny in the Mesozoic, which covered much of Arizona in volcanic debris and sediments. The Mid-Tertiary ignimbrite flare-up created smaller mountain ranges with extensive ash and lava in the Cenozoic, followed by the sinking of the Farallon slab in the mantle throughout the past 14 million years, which has created the Basin and Range Province. Arizona has extensive mineralization in veins, due to hydrothermal fluids and is notable for copper-gold porphyry, lead, zinc, rare minerals formed from copper enrichment and evaporites among other resources.

The geology of Alberta encompasses parts of the Canadian Rockies and thick sedimentary sequences, bearing coal, oil and natural gas, atop complex Precambrian crystalline basement rock.

<span class="mw-page-title-main">Geology of Wyoming</span>

The geology of Wyoming includes some of the oldest Archean rocks in North America, overlain by thick marine and terrestrial sediments formed during the Paleozoic, Mesozoic and Cenozoic, including oil, gas and coal deposits. Throughout its geologic history, Wyoming has been uplifted several times during the formation of the Rocky Mountains, which produced complicated faulting that traps hydrocarbons.

<span class="mw-page-title-main">Geology of Colorado</span>

The bedrock under the U.S. State of Colorado was assembled from island arcs accreted onto the edge of the ancient Wyoming Craton. The Sonoma orogeny uplifted the ancestral Rocky Mountains in parallel with the diversification of multicellular life. Shallow seas covered the regions, followed by the uplift current Rocky Mountains and intense volcanic activity. Colorado has thick sedimentary sequences with oil, gas and coal deposits, as well as base metals and other minerals.

<span class="mw-page-title-main">Geology of Nevada</span>

The geology of Nevada began to form in the Proterozoic at the western margin of North America. Terranes accreted to the continent as a marine environment dominated the area through the Paleozoic and Mesozoic periods. Intense volcanism, the horst and graben landscape of the Basin and Range Province originating from the Farallon Plate, and both glaciers and valley lakes have played important roles in the region throughout the past 66 million years.

The geology of Montana includes thick sequences of Paleozoic, Mesozoic and Cenozoic sedimentary rocks overlying ancient Archean and Proterozoic crystalline basement rock. Eastern Montana has considerable oil and gas resources, while the uplifted Rocky Mountains in the west, which resulted from the Laramide orogeny and other tectonic events have locations with metal ore.

The geology of Argentina includes ancient Precambrian basement rock affected by the Grenville orogeny, sediment filled basins from the Mesozoic and Cenozoic as well as newly uplifted areas in the Andes.

<span class="mw-page-title-main">Geology of the Kimberley (Western Australia)</span> Overview of geology of the Kimberley

The geology of the Kimberley, a region of Western Australia, is a rock record of the early Proterozoic eon that includes tectonic plate collision, mountain-building (orogeny) and the joining (suturing) of the Kimberley and Northern Australia cratons, followed by sedimentary basin formation.

References

  1. 1 2 3 4 5 English, Joseph M.; Johnston, Stephen T. (2004). "The Laramide Orogeny: What Were the Driving Forces?" (PDF). International Geology Review . 46 (9): 833–838. Bibcode:2004IGRv...46..833E. doi:10.2747/0020-6814.46.9.833. S2CID   129901811.
  2. ↑ Chamberlain, Kevin R., Carol D. Frost, and B. Ronald Frost (2003). "Early Archean to Mesoproterozoic evolution of the Wyoming Province: Archean origins to modern lithospheric architecture". Canadian Journal of Earth Sciences. 40 (10): 1357–1374. Bibcode:2003CaJES..40.1357C. doi:10.1139/e03-054.{{cite journal}}: CS1 maint: multiple names: authors list (link)
  3. 1 2 3 Sims, PK; Finn, CA; Rystrom, VL (2001). "Preliminary Precambrian Basement Map Showing Geologic-Geophysical Domains, Wyoming". Open-File Report 01-199. United States Geological Survey.
  4. ↑ Whitmeyer, Steven; Karlstrom, Karl E. (2007). "Tectonic model for the Proterozoic growth of North America". Geosphere. 3 (4): 220. doi: 10.1130/GES00055.1 .
  5. ↑ Foster, DA; Mueller, PA; Mogk, DW; Wooden, JL; Vogl, JJ (2006). "Proterozoic evolution of the western margin of the Wyoming craton: implications for the tectonic and magmatic evolution of the northern Rocky Mountains". Canadian Journal of Earth Sciences. 43 (10): 1601–1619. Bibcode:2006CaJES..43.1601F. doi:10.1139/e06-052.
  6. ↑ Willis, Grant (2021-09-13). "Utah's Great Unconformity". Survey Notes. Utah Geological Survey.
  7. ↑ Gadd, Ben (1995). Handbook of the Canadian Rockies. Corax Press. pp. 76–93. ISBN   9780969263111.
  8. 1 2 Kirk R. Johnson; Robert G. Raynolds (2006). Ancient Denvers: Scenes from the Past 300 Million Years of the Colorado Front Range. Fulcrum Publishing for Denver Museum of Nature and Science. ISBN   1-55591-554-X.
  9. ↑ Chronic, Halka (1980). Roadside Geology of Colorado. Mountain Press Publishing Company. ISBN   978-0-87842-105-3.
  10. ↑ Harris, Ann G.; Tuttle, Esther; Tuttle, Sherwood D (1997). Geology of National Parks (Fifth ed.). Iowa: Kendall/Hunt Publishing. pp. 566–567. ISBN   978-0-7872-5353-0.
  11. 1 2 Blakey, Ron. "Geologic History of Western US". Archived from the original on 2010-06-22.
  12. 1 2 3 4 5 PD-icon.svg This article incorporates public domain material from "Rocky Mountains". Geologic Provinces of the United States. United States Geological Survey. Archived from the original on 2006-09-22. Retrieved 2006-12-10.
  13. ↑ Jones, DL (1990). "Synopsis of late Palaeozoic and Mesozoic terrane accretion within the Cordillera of western North America". Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences. 331 (1620): 479–486. Bibcode:1990RSPTA.331..479J. doi:10.1098/rsta.1990.0084. S2CID   120813880.
  14. 1 2 3 Gadd, Ben (2008). Canadian Rockies Geology Road Tours. Corax Press. ISBN   9780969263128.
  15. ↑ Livaccari, RF; Burke, K; Sengor, AMC (1981). "Was the Laramide orogeny related to subduction of an oceanic plateau?". Nature. 289 (5795): 276–278. Bibcode:1981Natur.289..276L. doi:10.1038/289276a0. S2CID   27153755.
  16. 1 2 3 4 PD-icon.svg This article incorporates public domain material from Stohlgren, TJ. "Rocky Mountains". Status and Trends in the Nation's Biological Resources. United States Geological Survey. Archived from the original on 2006-09-27.
  17. ↑ Pierce, K. L. (1979). History and dynamics of glaciation in the northern Yellowstone National Park area. Washington, D.C: U.S. Geological Survey. pp. 1–90. Professional Paper 729-F.
  18. ↑ Gadd, Ben (2008). "Geology of the Rocky Mountains and Columbias" (PDF). Archived from the original (PDF) on 2012-04-02. Retrieved 2010-01-01.
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