Laurentia or the North American Craton is a large continental craton that forms the ancient geological core of the North American continent. Many times in its past, Laurentia has been a separate continent, as it is now in the form of North America, although originally it also included the cratonic areas of Greenland and also the northwestern part of Scotland, known as the Hebridean Terrane. During other times in its past, Laurentia has been part of larger continents and supercontinents and itself consists of many smaller terranes assembled on a network of Early Proterozoic orogenic belts. Small microcontinents and oceanic islands collided with and sutured onto the ever-growing Laurentia, and together formed the stable Precambrian craton seen today.

The craton is named after the Laurentian Shield, through the Laurentian Mountains, which received their name from the Saint Lawrence River, named after Lawrence of Rome.

In eastern and central Canada, much of the stable craton is exposed at the surface as the Canadian Shield; when subsurface extensions are considered, the wider term Laurentian Shield is more common, not least because large parts of the structure extend outside Canada. In the United States, the craton bedrock is covered with sedimentary rocks on the broad interior platform in the Midwest and Great Plains regions and is exposed only in northern Minnesota, Wisconsin, the New York Adirondacks, and the Upper Peninsula of Michigan. The sequence of rocks varies from about 1,000 m to in excess of 6,100 m (3,500–20,000 ft) in thickness. The cratonic rocks are metamorphic or igneous with the overlying sedimentary layers composed mostly of limestones, sandstones, and shales. These sedimentary rocks were largely deposited from 650 to 290 million years ago.

The metamorphic and igneous rocks of the "basement complex" of Laurentia were formed 1.5 to 1.0 billion years ago in a tectonically active setting. The younger sedimentary rocks that were deposited on top of this basement complex were formed in a setting of quiet marine and river waters. During much of Mississippian time, the craton was the site of an extensive marine carbonate platform on which mainly limestones and some dolostones and evaporites were deposited. This platform extended from either the present Appalachian Mountains or Mississippi Valley to the present Great Basin. The craton was covered by shallow, warm, tropical epicontinental or epicratonic sea (meaning literally "on the craton") that had maximum depths of only about 60 m (200 ft) at the shelf edge. During Cretaceous times, such a sea, the Western Interior Seaway, ran from the Gulf of Mexico to the Arctic Ocean, dividing North America into eastern and western land masses. Sometimes, land masses or mountain chains rose up on the distant edges of the craton and then eroded down, shedding their sand across the landscape. Subduction of the continent towards the Northwest, that lasted approximately 1.4 to 1.2 billion years, likely caused organic enrichment of the Grenvillian lithospheric mantle. This enrichment is thought to have contributed to the formation of the major supercontinent Rodinia.

The southwestern portion of Laurentia consists of Precambrian basement rocks deformed by continental collisions (violet area of the image above). This area has been subjected to considerable rifting as the Basin and Range Province and has been stretched up to 100% of its original width. The area contains numerous large volcanic eruptions.

The position of the equator during the Late Ordovician Epoch (c. 458 – c. 444 Ma) on Laurentia has been determined via expansive shell bed records. Flooding of the continent that occurred during the Ordovician provided the shallow warm waters for the success of sea life and therefore a spike in the carbonate shells of shellfish. Today the beds are composed of fossilized shells or massive-bedded Thalassinoides facies (MBTF) and loose shells or nonamalgamated brachiopod shell beds (NABS). These beds imply the presence of an equatorial climate belt that was hurricane free which lay inside 10° of the equator at 22.1°S ± 13.5°. This ecological conclusion matches the previous paleomagnetic findings which confirms this equatorial location.

This page was last edited on 16 June 2018, at 13:41.
Reference: under CC BY-SA license.

Related Topics

Recently Viewed