Michigan is a state in the Great Lakes and Midwestern regions of the United States. The state's name, originates from the Ojibwe word mishigamaa, meaning "large water" or "large lake". With a population of about 10 million, Michigan is the tenth most populous of the 50 United States, with the 11th most extensive total area, is the largest state by total area east of the Mississippi River, its capital is Lansing, its largest city is Detroit. Metro Detroit is among the nation's largest metropolitan economies. Michigan is the only state to consist of two peninsulas; the Lower Peninsula is noted as shaped like a mitten. The Upper Peninsula is separated from the Lower Peninsula by the Straits of Mackinac, a five-mile channel that joins Lake Huron to Lake Michigan; the Mackinac Bridge connects the peninsulas. The state has the longest freshwater coastline of any political subdivision in the world, being bounded by four of the five Great Lakes, plus Lake Saint Clair; as a result, it is one of the leading U.
S. states for recreational boating. Michigan has 64,980 inland lakes and ponds. A person in the state is never more than six miles from a natural water source or more than 85 miles from a Great Lakes shoreline; the area was first occupied by a succession of Native American tribes over thousands of years. Inhabited by Natives, Métis, French explorers in the 17th century, it was claimed as part of New France colony. After France's defeat in the French and Indian War in 1762, the region came under British rule. Britain ceded this territory to the newly independent United States after Britain's defeat in the American Revolutionary War; the area was part of the larger Northwest Territory until 1800, when western Michigan became part of the Indiana Territory. Michigan Territory was formed in 1805, but some of the northern border with Canada was not agreed upon until after the War of 1812. Michigan was admitted into the Union in 1837 as a free one, it soon became an important center of industry and trade in the Great Lakes region and a popular immigrant destination in the late 19th and early 20th centuries.
Although Michigan developed a diverse economy, it is known as the center of the U. S. automotive industry, which developed as a major economic force in the early 20th century. It is home to the country's three major automobile companies. While sparsely populated, the Upper Peninsula is important for tourism thanks to its abundance of natural resources, while the Lower Peninsula is a center of manufacturing, agriculture and high-tech industry; when the first European explorers arrived, the most populous tribes were Algonquian peoples, which include the Anishinaabe groups of Ojibwe, Odaawaa/Odawa, the Boodewaadamii/Bodéwadmi. The three nations co-existed peacefully as part of a loose confederation called the Council of Three Fires; the Ojibwe, whose numbers are estimated to have been between 25,000 and 35,000, were the largest. The Ojibwe were established in Michigan's Upper Peninsula and northern and central Michigan, inhabited Ontario and southern Manitoba, Canada; the Ottawa lived south of the Straits of Mackinac in northern and southern Michigan, but in southern Ontario, northern Ohio and eastern Wisconsin.
The Potawatomi were in southern and western Michigan, in addition to northern and central Indiana, northern Illinois, southern Wisconsin, southern Ontario. Other Algonquian tribes in Michigan, in the south and east, were the Mascouten, the Menominee, the Miami, the Sac, the Fox; the Wyandot were an Iroquoian-speaking people in this area. French voyageurs and coureurs des bois settled in Michigan in the 17th century; the first Europeans to reach what became Michigan were those of Étienne Brûlé's expedition in 1622. The first permanent European settlement was founded in 1668 on the site where Père Jacques Marquette established Sault Ste. Marie, Michigan as a base for Catholic missions. Missionaries in 1671–75 founded outlying stations at Saint Ignace and Marquette. Jesuit missionaries were well received by the area's Indian populations, with few difficulties or hostilities. In 1679, Robert Cavelier, Sieur de la Salle built Fort Miami at present-day St. Joseph. In 1691, the French established a trading post and Fort St. Joseph along the St. Joseph River at the present-day city of Niles.
In 1701, French explorer and army officer Antoine de la Mothe Cadillac founded Fort Pontchartrain du Détroit or "Fort Pontchartrain on-the-Strait" on the strait, known as the Detroit River, between lakes Saint Clair and Erie. Cadillac had convinced King Louis XIV's chief minister, Louis Phélypeaux, Comte de Pontchartrain, that a permanent community there would strengthen French control over the upper Great Lakes and discourage British aspirations; the hundred soldiers and workers who accompanied Cadillac built a fort enclosing one arpent and named it Fort Pontchartrain. Cadillac's wife, Marie Thérèse Guyon, soon moved to Detroit, becoming one of the first European women to settle in what was considered the wilderness of Michigan; the town became a major fur-trading and shipping post. The Église de Saint-Anne was founded the same year. While the original building does not survive, the congregation remains active. Cadillac departed to serve as the French governor of Louisiana from 1710 to 1716.
French attempts to consol
The Marcellus Formation is a Middle Devonian age unit of sedimentary rock found in eastern North America. Named for a distinctive outcrop near the village of Marcellus, New York, in the United States, it extends throughout much of the Appalachian Basin; the unit name usage by the U. S. Geological Survey includes Marcellus Formation; the term "Marcellus Shale" is the preferred name throughout most of the Appalachian region, although the term "Marcellus Formation" is acceptable within the State of Pennsylvania. The unit was first described and named as the "Marcellus shales" by J. Hall in 1839. Although black shale is the dominant lithology, it contains lighter shales and interbedded limestone layers; the Marcellus Formation is a black shale that may contain limestone beds and concentrations of iron pyrite and siderite. Its sedimentary structure, or bedding, is moderately well developed. Like most shales, it tends to split along the bedding plane, a property known as fissility. Lighter colored shales in the upper portion of the formation tend to split into small thin-edged fragments after exposure.
These fragments may have rust stains from exposure of pyrite to air, tiny gypsum crystals from the reaction between pyrite and limestone particles. Fresh exposures of the pyriteiferous shale may develop the secondary mineralization of orange limonite, the pale yellow efflorescence or bloom of sulfur, associated with acid rock drainage. Pyrite is abundant near the base, the upper contacts of limestones, but framboidal microcrystals and euhedral crystals of pyrite occur throughout the organic-rich deposits; the Marcellus contains uranium, the radioactive decay of the uranium-238 makes it a source rock for radioactive radon gas. Measured total organic content of the Marcellus Formation ranges from less than 1% in eastern New York, to over 11% in the central part of the state, the shale may contain enough carbon to support combustion; the more organic-rich black shales can be bituminous, but are too old to contain bituminous coal formed from land plants. In petroleum geology, these black shales are an important source rock that filled conventional petroleum reservoirs in overlying formations, are an unconventional shale gas reservoir, are an impermeable seal that traps underlying conventional natural gas reservoirs.
To the west the formation may produce liquid petroleum. The Marcellus is found throughout the Allegheny Plateau region of the northern Appalachian Basin of North America. In the United States, the Marcellus shale runs across the Southern Tier and Finger Lakes regions of New York, in northern and western Pennsylvania, eastern Ohio, through western Maryland, throughout most of West Virginia extending across the state line into extreme western Virginia; the Marcellus bedrock in eastern Pennsylvania extends across the Delaware River into extreme western New Jersey. It exists in the subsurface of a small portion of Kentucky and Tennessee. Below Lake Erie, it can be found crossing the border into Canada, where it stretches between Port Stanley and Long Point to St. Thomas in southern Ontario; the Marcellus appears in outcrops along the northern margin of the formation in central New York. There, the two joint planes in the Marcellus are nearly at right angles, each making cracks in the formation that run perpendicular to the bedding plane, which lies level.
These joints form smooth nearly vertical cliffs, the intersecting joint planes form projecting corners in the rock faces. Once exposed, the weathered faces lose most of their organic carbon, turning from black or dark gray to a lighter shade of gray. Outcrops of the Marcellus can contain small beds that resemble coal; the New York outcrops, others further south in Pennsylvania and New Jersey, were extensively excavated in the early 19th century, sometimes at great expense, in the false hope of finding minable coal seams. In Perry County, Pennsylvania along the Juniata River the false coal beds become up to.3 m thick, but they did not produce a valuable fuel, despite the considerable effort expended to mine it from the surrounding hills. Seaweed and marine plants formed the false coal. True coal is formed from terrestrial plants, which only began to appear in Marcellus and fossils. Close proximity to the surface of Marcellus bedrock south of the New York outcrops makes an east-west band running through the city of Syracuse a high-risk area for radon as an indoor air pollutant.
From the surface exposures along the northern and eastern margins, the formation descends to depths of over 2,700 m below the surface in southern Pennsylvania. Upturned beds are exposed in sections of the folded Ridge-and-Valley Appalachians, including exposures on the flanks and axis of the Broad Top Synclinorium in south central Pennsylvania. Exposed beds are nearly horizontal on the Allegheny Plateau, but upturned to form overturned beds found along the Allegheny Front. From Wind Gap, Pennsylvania heading south, the dip of the beds steepens, becoming vertical at Bowmanstown on the Lehigh River. Nearby, in the Lehigh Gap area of Pennsylvania, the Marcellus is extensively faulted, the beds are steeply overturned, with a reverse dip angle of up to 40° south; the Marcellus Shale and the fine-grained shales near the middle of the Mahantango Formation are classified by geologists as slope-formers. Marcellus and Mahantango shale beds dipping at 60° to 75° to the west form the west facing slopes of Tonoloway Ridge on the wes
The Carboniferous is a geologic period and system that spans 60 million years from the end of the Devonian Period 358.9 million years ago, to the beginning of the Permian Period, 298.9 Mya. The name Carboniferous means "coal-bearing" and derives from the Latin words carbō and ferō, was coined by geologists William Conybeare and William Phillips in 1822. Based on a study of the British rock succession, it was the first of the modern'system' names to be employed, reflects the fact that many coal beds were formed globally during that time; the Carboniferous is treated in North America as two geological periods, the earlier Mississippian and the Pennsylvanian. Terrestrial animal life was well established by the Carboniferous period. Amphibians were the dominant land vertebrates, of which one branch would evolve into amniotes, the first terrestrial vertebrates. Arthropods were very common, many were much larger than those of today. Vast swaths of forest covered the land, which would be laid down and become the coal beds characteristic of the Carboniferous stratigraphy evident today.
The atmospheric content of oxygen reached its highest levels in geological history during the period, 35% compared with 21% today, allowing terrestrial invertebrates to evolve to great size. The half of the period experienced glaciations, low sea level, mountain building as the continents collided to form Pangaea. A minor marine and terrestrial extinction event, the Carboniferous rainforest collapse, occurred at the end of the period, caused by climate change. In the United States the Carboniferous is broken into Mississippian and Pennsylvanian subperiods; the Mississippian is about twice as long as the Pennsylvanian, but due to the large thickness of coal-bearing deposits with Pennsylvanian ages in Europe and North America, the two subperiods were long thought to have been more or less equal in duration. In Europe the Lower Carboniferous sub-system is known as the Dinantian, comprising the Tournaisian and Visean Series, dated at 362.5-332.9 Ma, the Upper Carboniferous sub-system is known as the Silesian, comprising the Namurian and Stephanian Series, dated at 332.9-298.9 Ma.
The Silesian is contemporaneous with the late Mississippian Serpukhovian plus the Pennsylvanian. In Britain the Dinantian is traditionally known as the Carboniferous Limestone, the Namurian as the Millstone Grit, the Westphalian as the Coal Measures and Pennant Sandstone; the International Commission on Stratigraphy faunal stages from youngest to oldest, together with some of their regional subdivisions, are: A global drop in sea level at the end of the Devonian reversed early in the Carboniferous. There was a drop in south polar temperatures; these conditions had little effect in the deep tropics, where lush swamps to become coal, flourished to within 30 degrees of the northernmost glaciers. Mid-Carboniferous, a drop in sea level precipitated a major marine extinction, one that hit crinoids and ammonites hard; this sea level drop and the associated unconformity in North America separate the Mississippian subperiod from the Pennsylvanian subperiod. This happened about 323 million years ago, at the onset of the Permo-Carboniferous Glaciation.
The Carboniferous was a time of active mountain-building as the supercontinent Pangaea came together. The southern continents remained tied together in the supercontinent Gondwana, which collided with North America–Europe along the present line of eastern North America; this continental collision resulted in the Hercynian orogeny in Europe, the Alleghenian orogeny in North America. In the same time frame, much of present eastern Eurasian plate welded itself to Europe along the line of the Ural Mountains. Most of the Mesozoic supercontinent of Pangea was now assembled, although North China, South China continents were still separated from Laurasia; the Late Carboniferous Pangaea was shaped like an "O." There were two major oceans in the Carboniferous—Panthalassa and Paleo-Tethys, inside the "O" in the Carboniferous Pangaea. Other minor oceans were shrinking and closed - Rheic Ocean, the small, shallow Ural Ocean and Proto-Tethys Ocean. Average global temperatures in the Early Carboniferous Period were high: 20 °C.
However, cooling during the Middle Carboniferous reduced average global temperatures to about 12 °C. Lack of growth rings of fossilized trees suggest a lack of seasons of a tropical climate. Glaciations in Gondwana, triggered by Gondwana's southward movement, continued into the Permian and because of the lack of clear markers and breaks, the deposits of this glacial period are referred to as Permo-Carboniferous in age; the cooling and drying of the climate led to the Carboniferous Rainforest Collapse during the late Carboniferous. Tropical rainforests fragmented and were devastated by climate change. Carboniferous rocks in Europe and eastern North America consist of a repeated sequence of limestone, sandstone and coal beds. In North America, the early Carboniferous is marine
West Falls Formation
The West Falls Group is a geologic group in New York. It preserves fossils dating back to the Devonian period; the West Falls formation is bounded above by the Java Formation and below by the Sonyea Formation. It comprises the Angola Rhinestreet Shale Members, it is part of the Salina thrust sheet. The Rhinestreet Shale and Angola Shale Members of the West Falls Formation are both recognized in the subsurface from western New York to eastern Tennessee; the predominant lithology of the West Falls Group is shale. The Rhinestreet Member can be further subdivided into two shale types: a thick, fissile black shale underlies a gray to greenish-gray shale that indicates a transitional environment; the Angola member is a gray to greenish-gray shale distinguished by its consistent low gamma ray signature, typical of this shale type. The West Falls Formation was deposited during the Frasnian stage of the Upper Devonian. Two distinct community types are observed in the group: "a shallower water spiriferacean-rhynchonellide-bivalve species ensemble, a deeper water assemblage of unattached epibenthic and sessile semi-infaunal brachiopods".
Both members of the West Falls Formation have been assessed for gas exploration. The USGS has determined that the average total organic carbon in the Rhinestreet Shale is 0.89%. The Rathbone shale field in Rathbone, Steuben County, New York was discovered in 1931. 31 wells were drilled in this field, targeting the Rhinestreet members. Of these, 24 produced natural gas, 4 were dry holes, 2 were plugged and abandoned, one produced oil; the wells were 900- 1,500 feet in depth, reservoir pressure was 225 psi and flow rates ranged from 100-2,000 Mcfd. List of fossiliferous stratigraphic units in New York Various Contributors to the Paleobiology Database. "Fossilworks: Gateway to the Paleobiology Database". Retrieved 22 June 2014. Rickard, L. V.. W.. W.. "Geologic map of New York: Finger Lakes sheet". New York State Museum. Retrieved 2015-09-17. Http://pubs.usgs.gov/imap/i2791/FIG3.pdf https://mrdata.usgs.gov/geology/state/sgmc-unit.php?unit=NYDwf%3B4 http://www.dnr.state.oh.us/Portals/10/pdf/OpenFileReports/OFR_88-3.pdf http://treichlerlawoffice.com/radiation/HillNY.pdf
The Permian is a geologic period and system which spans 47 million years from the end of the Carboniferous Period 298.9 million years ago, to the beginning of the Triassic period 251.902 Mya. It is the last period of the Paleozoic era; the concept of the Permian was introduced in 1841 by geologist Sir Roderick Murchison, who named it after the city of Perm. The Permian witnessed the diversification of the early amniotes into the ancestral groups of the mammals, turtles and archosaurs; the world at the time was dominated by two continents known as Pangaea and Siberia, surrounded by a global ocean called Panthalassa. The Carboniferous rainforest collapse left behind vast regions of desert within the continental interior. Amniotes, who could better cope with these drier conditions, rose to dominance in place of their amphibian ancestors; the Permian ended with the Permian–Triassic extinction event, the largest mass extinction in Earth's history, in which nearly 96% of marine species and 70% of terrestrial species died out.
It would take well into the Triassic for life to recover from this catastrophe. Recovery from the Permian–Triassic extinction event was protracted; the term "Permian" was introduced into geology in 1841 by Sir R. I. Murchison, president of the Geological Society of London, who identified typical strata in extensive Russian explorations undertaken with Édouard de Verneuil; the region now lies in the Perm Krai of Russia. Official ICS 2017 subdivisions of the Permian System from most recent to most ancient rock layers are: Lopingian epoch Changhsingian Wuchiapingian Others: Waiitian Makabewan Ochoan Guadalupian epoch Capitanian stage Wordian stage Roadian stage Others: Kazanian or Maokovian Braxtonian stage Cisuralian epoch Kungurian stage Artinskian stage Sakmarian stage Asselian stage Others: Telfordian Mangapirian Sea levels in the Permian remained low, near-shore environments were reduced as all major landmasses collected into a single continent—Pangaea; this could have in part caused the widespread extinctions of marine species at the end of the period by reducing shallow coastal areas preferred by many marine organisms.
During the Permian, all the Earth's major landmasses were collected into a single supercontinent known as Pangaea. Pangaea straddled the equator and extended toward the poles, with a corresponding effect on ocean currents in the single great ocean, the Paleo-Tethys Ocean, a large ocean that existed between Asia and Gondwana; the Cimmeria continent rifted away from Gondwana and drifted north to Laurasia, causing the Paleo-Tethys Ocean to shrink. A new ocean was growing on its southern end, the Tethys Ocean, an ocean that would dominate much of the Mesozoic era. Large continental landmass interiors experience climates with extreme variations of heat and cold and monsoon conditions with seasonal rainfall patterns. Deserts seem to have been widespread on Pangaea; such dry conditions favored gymnosperms, plants with seeds enclosed in a protective cover, over plants such as ferns that disperse spores in a wetter environment. The first modern trees appeared in the Permian. Three general areas are noted for their extensive Permian deposits—the Ural Mountains and the southwest of North America, including the Texas red beds.
The Permian Basin in the U. S. states of Texas and New Mexico is so named because it has one of the thickest deposits of Permian rocks in the world. The climate in the Permian was quite varied. At the start of the Permian, the Earth was still in an ice age. Glaciers receded around the mid-Permian period as the climate warmed, drying the continent's interiors. In the late Permian period, the drying continued although the temperature cycled between warm and cool cycles. Permian marine deposits are rich in fossil mollusks and brachiopods. Fossilized shells of two kinds of invertebrates are used to identify Permian strata and correlate them between sites: fusulinids, a kind of shelled amoeba-like protist, one of the foraminiferans, ammonoids, shelled cephalopods that are distant relatives of the modern nautilus. By the close of the Permian, trilobites and a host of other marine groups became extinct. Terrestrial life in the Permian included diverse plants, fungi and various types of tetrapods; the period saw a massive desert covering the interior of Pangaea.
The warm zone spread in the northern hemisphere. The rocks formed at that time were stained red by iron oxides, the result of intense heating by the sun of a surface devoid of vegetation cover. A number of older types of plants and animals became marginal elements; the Permian began with the Carboniferous flora still flourishing. About the middle of the Permian a major transition in vegetation began; the swamp-loving
The Devonian is a geologic period and system of the Paleozoic, spanning 60 million years from the end of the Silurian, 419.2 million years ago, to the beginning of the Carboniferous, 358.9 Mya. It is named after Devon, where rocks from this period were first studied; the first significant adaptive radiation of life on dry land occurred during the Devonian. Free-sporing vascular plants began to spread across dry land, forming extensive forests which covered the continents. By the middle of the Devonian, several groups of plants had evolved leaves and true roots, by the end of the period the first seed-bearing plants appeared. Various terrestrial arthropods became well-established. Fish reached substantial diversity during this time, leading the Devonian to be dubbed the "Age of Fishes." The first ray-finned and lobe-finned bony fish appeared, while the placoderms began dominating every known aquatic environment. The ancestors of all four-limbed vertebrates began adapting to walking on land, as their strong pectoral and pelvic fins evolved into legs.
In the oceans, primitive sharks became more numerous than in the Late Ordovician. The first ammonites, species of molluscs, appeared. Trilobites, the mollusc-like brachiopods and the great coral reefs, were still common; the Late Devonian extinction which started about 375 million years ago affected marine life, killing off all placodermi, all trilobites, save for a few species of the order Proetida. The palaeogeography was dominated by the supercontinent of Gondwana to the south, the continent of Siberia to the north, the early formation of the small continent of Euramerica in between; the period is named after Devon, a county in southwestern England, where a controversial argument in the 1830s over the age and structure of the rocks found distributed throughout the county was resolved by the definition of the Devonian period in the geological timescale. The Great Devonian Controversy was a long period of vigorous argument and counter-argument between the main protagonists of Roderick Murchison with Adam Sedgwick against Henry De la Beche supported by George Bellas Greenough.
Murchison and Sedgwick named the period they proposed as the Devonian System. While the rock beds that define the start and end of the Devonian period are well identified, the exact dates are uncertain. According to the International Commission on Stratigraphy, the Devonian extends from the end of the Silurian 419.2 Mya, to the beginning of the Carboniferous 358.9 Mya. In nineteenth-century texts the Devonian has been called the "Old Red Age", after the red and brown terrestrial deposits known in the United Kingdom as the Old Red Sandstone in which early fossil discoveries were found. Another common term is "Age of the Fishes", referring to the evolution of several major groups of fish that took place during the period. Older literature on the Anglo-Welsh basin divides it into the Downtonian, Dittonian and Farlovian stages, the latter three of which are placed in the Devonian; the Devonian has erroneously been characterised as a "greenhouse age", due to sampling bias: most of the early Devonian-age discoveries came from the strata of western Europe and eastern North America, which at the time straddled the Equator as part of the supercontinent of Euramerica where fossil signatures of widespread reefs indicate tropical climates that were warm and moderately humid but in fact the climate in the Devonian differed during its epochs and between geographic regions.
For example, during the Early Devonian, arid conditions were prevalent through much of the world including Siberia, North America, China, but Africa and South America had a warm temperate climate. In the Late Devonian, by contrast, arid conditions were less prevalent across the world and temperate climates were more common; the Devonian Period is formally broken into Early and Late subdivisions. The rocks corresponding to those epochs are referred to as belonging to the Lower and Upper parts of the Devonian System. Early DevonianThe Early Devonian lasted from 419.2 ± 2.8 to 393.3 ± 2.5 and began with the Lochkovian stage, which lasted until the Pragian. It spanned from 410.8 ± 2.8 to 407.6 ± 2.5, was followed by the Emsian, which lasted until the Middle Devonian began, 393.3± 2.7 million years ago. During this time, the first ammonoids appeared. Ammonoids during this time period differed little from their nautiloid counterparts; these ammonoids belong to the order Agoniatitida, which in epochs evolved to new ammonoid orders, for example Goniatitida and Clymeniida.
This class of cephalopod molluscs would dominate the marine fauna until the beginning of the Mesozoic era. Middle DevonianThe Middle Devonian comprised two subdivisions: first the Eifelian, which gave way to the Givetian 387.7± 2.7 million years ago. During this time the jawless agnathan fishes began to decline in diversity in freshwater and marine environments due to drastic environmental changes and due to the increasing competition and diversity of jawed fishes; the shallow, oxygen-depleted waters of Devonian inland lakes, surrounded by primitive plants, provided the environment necessary for certain early fish to develop such essential characteristics as well developed lungs, the ability to crawl out of the water and onto the land for short periods of time. Late DevonianFinally, the Late Devonian started with the Frasnian, 382.7 ± 2.8 to 372.2 ± 2.5, during which the first forests took shape on land. The first tetrapods appeared in the fossil record in the ensuing Famennian subdivisi