Hamlin Peak is a 4,756-foot mountain located in Baxter State Park in Piscataquis County, Maine. Hamlin Peak is a northern spur of the greater Mount Katahdin massif and is flanked to the south by Baxter Peak, to the north by the Howe Peaks. Since it rises nearly 500 feet above the col joining it to the higher Baxter Peak, Hamlin Peak qualifies as a four-thousand footer based on the topographic prominence criterion used by the Appalachian Mountain Club, is ranked as the second-highest peak in Maine; the southeast face of Hamlin Peak drains into the Great Basin, where water flows into the Penobscot River and empties into the Atlantic Ocean at Penobscot Bay. There are several trails. List of mountains in Maine
Lava is molten rock generated by geothermal energy and expelled through fractures in planetary crust or in an eruption at temperatures from 700 to 1,200 °C. The structures resulting from subsequent solidification and cooling are sometimes described as lava; the molten rock is formed in the interior of some planets, including Earth, some of their satellites, though such material located below the crust is referred to by other terms. A lava flow is a moving outpouring of lava created during a non-explosive effusive eruption; when it has stopped moving, lava solidifies to form igneous rock. The term lava flow is shortened to lava. Although lava can be up to 100,000 times more viscous than water, lava can flow great distances before cooling and solidifying because of its thixotropic and shear thinning properties. Explosive eruptions produce a mixture of volcanic ash and other fragments called tephra, rather than lava flows; the word lava comes from Italian, is derived from the Latin word labes which means a fall or slide.
The first use in connection with extruded magma was in a short account written by Francesco Serao on the eruption of Vesuvius in 1737. Serao described "a flow of fiery lava" as an analogy to the flow of water and mud down the flanks of the volcano following heavy rain; the composition of all lava of the Earth's crust is dominated by silicate minerals feldspars, pyroxenes, amphiboles and quartz. Igneous rocks, which form lava flows when erupted, can be classified into three chemical types: felsic and mafic; these classes are chemical, the chemistry of lava tends to correlate with the magma temperature, its viscosity and its mode of eruption. Felsic or silicic lavas such as rhyolite and dacite form lava spines, lava domes or "coulees" and are associated with pyroclastic deposits. Most silicic lava flows are viscous, fragment as they extrude, producing blocky autobreccias; the high viscosity and strength are the result of their chemistry, high in silica, potassium and calcium, forming a polymerized liquid rich in feldspar and quartz, thus has a higher viscosity than other magma types.
Felsic magmas can erupt at temperatures as low as 650 to 750 °C. Unusually hot rhyolite lavas, may flow for distances of many tens of kilometres, such as in the Snake River Plain of the northwestern United States. Intermediate or andesitic lavas are lower in aluminium and silica, somewhat richer in magnesium and iron. Intermediate lavas form andesite domes and block lavas, may occur on steep composite volcanoes, such as in the Andes. Poorer in aluminium and silica than felsic lavas, commonly hotter, they tend to be less viscous. Greater temperatures tend to destroy polymerized bonds within the magma, promoting more fluid behaviour and a greater tendency to form phenocrysts. Higher iron and magnesium tends to manifest as a darker groundmass, occasionally amphibole or pyroxene phenocrysts. Mafic or basaltic lavas are typified by their high ferromagnesian content, erupt at temperatures in excess of 950 °C. Basaltic magma is high in iron and magnesium, has lower aluminium and silica, which taken together reduces the degree of polymerization within the melt.
Owing to the higher temperatures, viscosities can be low, although still thousands of times higher than water. The low degree of polymerization and high temperature favors chemical diffusion, so it is common to see large, well-formed phenocrysts within mafic lavas. Basalt lavas tend to produce low-profile shield volcanoes or "flood basalt fields", because the fluidal lava flows for long distances from the vent; the thickness of a basalt lava on a low slope, may be much greater than the thickness of the moving lava flow at any one time, because basalt lavas may "inflate" by supply of lava beneath a solidified crust. Most basalt lavas are of pāhoehoe types, rather than block lavas. Underwater, they can form pillow lavas, which are rather similar to entrail-type pahoehoe lavas on land. Ultramafic lavas such as komatiite and magnesian magmas that form boninite take the composition and temperatures of eruptions to the extreme. Komatiites contain over 18% magnesium oxide, are thought to have erupted at temperatures of 1,600 °C.
At this temperature there is no polymerization of the mineral compounds, creating a mobile liquid. Most if not all ultramafic lavas are no younger than the Proterozoic, with a few ultramafic magmas known from the Phanerozoic. No modern komatiite lavas are known, as the Earth's mantle has cooled too much to produce magnesian magmas; some lavas of unusual composition have erupted onto the surface of the Earth. These include: Carbonatite and natrocarbonatite lavas are known from Ol Doinyo Lengai volcano in Tanzania, the sole example of an active carbonatite volcano. Iron oxide lavas are thought to be the source of the iron ore at Kiruna, Sweden which formed during the Proterozoic. Iron oxide lavas of Pliocene age occur at the El Laco volcanic complex on the Chile-Argentina border. Iron oxide lavas are thought to be the result of immiscible separation of iron oxide magma from a parental magma of calc-alkaline or alkaline composition. Sulfur lava flows up to 250 metres 10 metres wide occur at Lastarria volcano, Chile.
They were formed by the melting of sulfur deposits at temperatures as low as 113 °C
The Appalachian National Scenic Trail known as the Appalachian Trail or the A. T. is a marked hiking trail in the Eastern United States extending between Springer Mountain in Georgia and Mount Katahdin in Maine. The trail is about 2,200 miles long, though the exact length changes over time as parts are modified or rerouted; the Appalachian Trail Conservancy describes the Appalachian Trail as the longest hiking-only trail in the world. More than 2 million people are said to take a hike on part of the trail at least once each year; the idea of the Appalachian Trail came about in 1921. The trail itself was completed in 1937 after more than a decade of work, although improvements and changes continue, it is maintained by 31 trail clubs and multiple partnerships, managed by the National Park Service, United States Forest Service, the nonprofit Appalachian Trail Conservancy. Most of the trail is in forest or wild lands, although some portions traverse towns and farms, it passes through 14 states: Georgia, North Carolina, Virginia, West Virginia, Pennsylvania, New Jersey, New York, Massachusetts, New Hampshire, Maine.
Thru-hikers attempt to hike the trail in its entirety in a single season. The number of thru-hikes per year has increased with 715 northbound and 133 southbound thru-hikes reported for 2017. Many books, documentaries and fan organizations are dedicated to the pursuit; some hike from one end to the other turn around and thru-hike the trail the other way, known as a "yo-yo". An extension known as the International Appalachian Trail continues northeast, crossing Maine and cutting through Canada to Newfoundland, with sections continuing in Greenland, through Europe, into Morocco. Other separate extensions continue the southern end of the Appalachian range in Alabama and continue south into Florida, creating what is known as the Eastern Continental Trail; the Appalachian Trail, the Continental Divide Trail, the Pacific Crest Trail form what is known as the Triple Crown of Hiking in the United States. The trail was conceived by Benton MacKaye, a forester who wrote his original plan—called "An Appalachian Trail, A Project in Regional Planning"—shortly after the death of his wife in 1921.
MacKaye's idea detailed a grand trail that would connect a series of farms and wilderness work/study camps for city-dwellers. In 1922, at the suggestion of Major William A. Welch, director of the Palisades Interstate Park Commission, his idea was publicized by Raymond H. Torrey with a story in the New York Evening Post under a full-page banner headline reading "A Great Trail from Maine to Georgia!" The idea was adopted by the new Palisades Interstate Park Trail Conference as their main project. On October 7, 1923, the first section of the trail, from Bear Mountain west through Harriman State Park to Arden, New York, was opened. MacKaye called for a two-day Appalachian Trail conference to be held in March 1925 in Washington, D. C; this meeting inspired the formation of the Appalachian Trail Conference. A retired judge named Arthur Perkins and his younger associate Myron Avery took up the cause. In 1929, a member of the Connecticut Forest and Park Association and its Blue Blazed Trails committee, found Ned Anderson, a farmer in Sherman, who took on the task of mapping and blazing the Connecticut leg of the trail.
It ran from Dog Tail Corners in Webatuck, New York, which borders Kent, Connecticut, at Ashley Falls, 50 miles through the northwest corner of the state, up to Bear Mountain at the Massachusetts border. Anderson's efforts helped spark renewed interest in the trail, Avery was able to bring other states on board. Upon taking over the ATC, Avery adopted the more practical goal of building a simple hiking trail, he and MacKaye clashed over the ATC's response to a major commercial development along the trail's path. Avery reigned as Chairman of the ATC from 1932 to 1952. Avery became the first to walk the trail end-to-end, though not as a thru-hike, in 1936. In August 1937, the trail was completed to Sugarloaf Mountain in Maine, the ATC shifted its focus toward protecting the trail lands and mapping the trail for hikers. Many of the trail's present highlights were not part of the trail in 1937: Roan Mountain, North Carolina and Tennessee. Except for places where the Civilian Conservation Corps was brought in, the original trail climbed straight up and down mountains, creating rough hiking conditions and a treadway prone to severe erosion.
The ATC's trail crews and volunteer trail-maintaining clubs have relocated or rehabilitated miles of trail since that time. In 1936, a 121-day Maine to Georgia veteran's group funded and supported thru-hike was reported to have been completed, with all but three miles of the new trail cleared and blazed, by six Boy Scouts from New York City and their guides; the completed thru-hike was much recorded and accepted by the Appalachian Long Distance Hikers Association. In 1938, the trail sustained major damage from a hurricane; this happened right before the start of World War II
Native Americans in the United States
Native Americans known as American Indians, Indigenous Americans and other terms, are the indigenous peoples of the United States, except Hawaii. There are over 500 federally recognized tribes within the US, about half of which are associated with Indian reservations; the term "American Indian" excludes Native Hawaiians and some Alaska Natives, while Native Americans are American Indians, plus Alaska Natives of all ethnicities. Native Hawaiians are not counted as Native Americans by the US Census, instead being included in the Census grouping of "Native Hawaiian and other Pacific Islander"; the ancestors of modern Native Americans arrived in what is now the United States at least 15,000 years ago much earlier, from Asia via Beringia. A vast variety of peoples and cultures subsequently developed. Native Americans were affected by the European colonization of the Americas, which began in 1492, their population declined precipitously due to introduced diseases as well as warfare, territorial confiscation and slavery.
After the founding of the United States, many Native American peoples were subjected to warfare and one-sided treaties, they continued to suffer from discriminatory government policies into the 20th century. Since the 1960s, Native American self-determination movements have resulted in changes to the lives of Native Americans, though there are still many contemporary issues faced by Native Americans. Today, there are over five million Native Americans in the United States, 78% of whom live outside reservations; when the United States was created, established Native American tribes were considered semi-independent nations, as they lived in communities separate from British settlers. The federal government signed treaties at a government-to-government level until the Indian Appropriations Act of 1871 ended recognition of independent native nations, started treating them as "domestic dependent nations" subject to federal law; this law did preserve the rights and privileges agreed to under the treaties, including a large degree of tribal sovereignty.
For this reason, many Native American reservations are still independent of state law and actions of tribal citizens on these reservations are subject only to tribal courts and federal law. The Indian Citizenship Act of 1924 granted U. S. citizenship to all Native Americans born in the United States. This emptied the "Indians not taxed" category established by the United States Constitution, allowed natives to vote in state and federal elections, extended the Fourteenth Amendment protections granted to people "subject to the jurisdiction" of the United States. However, some states continued to deny Native Americans voting rights for several decades. Bill of Rights protections do not apply to tribal governments, except for those mandated by the Indian Civil Rights Act of 1968. Since the end of the 15th century, the migration of Europeans to the Americas has led to centuries of population and agricultural transfer and adjustment between Old and New World societies, a process known as the Columbian exchange.
As most Native American groups had preserved their histories by oral traditions and artwork, the first written sources of the conflict were written by Europeans. Ethnographers classify the indigenous peoples of North America into ten geographical regions with shared cultural traits, called cultural areas; some scholars combine the Plateau and Great Basin regions into the Intermontane West, some separate Prairie peoples from Great Plains peoples, while some separate Great Lakes tribes from the Northeastern Woodlands. The ten cultural areas are as follows: Arctic, including Aleut and Yupik peoples Subarctic Northeastern Woodlands Southeastern Woodlands Great Plains Great Basin Northwest Plateau Northwest Coast California Southwest At the time of the first contact, the indigenous cultures were quite different from those of the proto-industrial and Christian immigrants; some Northeastern and Southwestern cultures, in particular, were matrilineal and operated on a more collective basis than that with which Europeans were familiar.
The majority of Indigenous American tribes maintained their hunting grounds and agricultural lands for use of the entire tribe. Europeans at that time had patriarchal cultures and had developed concepts of individual property rights with respect to land that were different; the differences in cultures between the established Native Americans and immigrant Europeans, as well as shifting alliances among different nations in times of war, caused extensive political tension, ethnic violence, social disruption. Before the European settlement of what is now the United States, Native Americans suffered high fatalities from contact with new European diseases, to which they had not yet acquired immunity. Smallpox epidemics are thought to have caused the greatest loss of life for indigenous populations. William M Denevan, noted author and Professor Emeritus of Geography at the University of Wisconsin-Madison, said on this subject in his essay "The Pristine Myth: The Landscape of the Americas in 1492".
Old World diseases were the primary killer. In many regions the tropical lowlands, populations fell by 90 percent or more in the first century after the contact. "Estimates of the pre-Columbian population of what today constitutes the U. S. vary ranging from William M Denevan's 3.8 million in his 1992 w
Rhyolite is an igneous, volcanic rock, of felsic composition. It may have any texture from glassy to aphanitic to porphyritic; the mineral assemblage is quartz and plagioclase. Biotite and hornblende are common accessory minerals, it is the extrusive equivalent to granite. Rhyolite can be considered as the extrusive equivalent to the plutonic granite rock, outcrops of rhyolite may bear a resemblance to granite. Due to their high content of silica and low iron and magnesium contents, rhyolitic magmas form viscous lavas, they occur as breccias or in volcanic plugs and dikes. Rhyolites that cool too to grow crystals form a natural glass or vitrophyre called obsidian. Slower cooling forms microscopic crystals in the lava and results in textures such as flow foliations, spherulitic and lithophysal structures; some rhyolite is vesicular pumice. Many eruptions of rhyolite are explosive and the deposits may consist of fallout tephra/tuff or of ignimbrites. Eruptions of rhyolite are rare compared to eruptions of less felsic lavas.
Only three eruptions of rhyolite have been recorded since the start of the 20th century: at the St. Andrew Strait volcano in Papua New Guinea, Novarupta volcano in Alaska, Chaiten in southern Chile. Rhyolite has been found on islands far from land. Etsch Valley Vulcanite Group near Bolzano and the surrounding area Gréixer rhyolitic complex at Moixeró range Vosges Iceland: all active and extinct central volcanoes, e.g. Torfajökull, Leirhnjúkur / Krafla, Breiddalur central volcano Papa Stour in Shetland Copper Coast Geopark in southeast Ireland various locations around Snowdonia, Wales Massif de l'Esterel, France the Thuringian Forest consists of rhyolites and pyroclastic rocks of the Rotliegendes Saxony the north west Saxony-Anhalt north of Halle Saar-Nahe Basin e.g. the Königstuhl on the Donnersberg mountain Black Forest e.g. on the Karlsruher Grat Odenwald Andes Cascade Range Cobalt, Ontario Sheep Creek, Idaho Rocky Mountains Jemez Mountains Rhyolite, Nevada was named after a rhyolite deposit that characterised the area.
Wichita Mountains within the Southern Oklahoma Aulacogen St. Francois Mountains Mount Jasper, New Hampshire Yellowstone Crater Lake, Oregon Palisade Head, a formation found at Tettegouche State Park, Minnesota; the Taupo Volcanic Zone in New Zealand has a large concentration of young rhyolite volcanoes Glass House Mountains National Park, Australia the Gondwana Rainforests of Australia World Heritage Area contains rhyolite-restricted flora along the Great Dividing Range the Flinders Peak Group in the Teviot Range in the Fassifern Valley is a rhyolite of varying colours. The Malani Igneous Suite, India; the Yandang Shan mountain chain, near the town of Wenzhou, Zhejiang province, China Tambora, Indonesia Mount Kilimanjaro, Kenya/Tanzania The name rhyolite was introduced into geology in 1860 by the German traveler and geologist Ferdinand von Richthofen from the Greek word rhýax and the rock name suffix "-lite". In North American pre-historic times, rhyolite was quarried extensively in eastern Pennsylvania in the United States.
Among the leading quarries was the Carbaugh Run Rhyolite Quarry Site in Adams County. Rhyolite was mined there starting 11,500 years ago. Tons of rhyolite were traded across the Delmarva Peninsula, because the rhyolite kept a sharp point when knapped and was used to make spear points and arrowheads. Comendite – A hard, peralkaline igneous rock, a type of light blue grey rhyolite List of rock types – A list of rock types recognized by geologists Pantellerite – A peralkaline rhyolite type of volcanic rock Thunderegg – A nodule-like rock, formed within rhyolitic volcanic ash layers University of North Dakota description of rhyolite Information from rocks-rock.com
Granite is a common type of felsic intrusive igneous rock, granular and phaneritic in texture. Granites can be predominantly white, pink, or gray depending on their mineralogy; the word "granite" comes from the Latin granum, a grain, in reference to the coarse-grained structure of such a holocrystalline rock. Speaking, granite is an igneous rock with between 20% and 60% quartz by volume, at least 35% of the total feldspar consisting of alkali feldspar, although the term "granite" is used to refer to a wider range of coarse-grained igneous rocks containing quartz and feldspar; the term "granitic" means granite-like and is applied to granite and a group of intrusive igneous rocks with similar textures and slight variations in composition and origin. These rocks consist of feldspar, quartz and amphibole minerals, which form an interlocking, somewhat equigranular matrix of feldspar and quartz with scattered darker biotite mica and amphibole peppering the lighter color minerals; some individual crystals are larger than the groundmass, in which case the texture is known as porphyritic.
A granitic rock with a porphyritic texture is known as a granite porphyry. Granitoid is a descriptive field term for lighter-colored, coarse-grained igneous rocks. Petrographic examination is required for identification of specific types of granitoids; the extrusive igneous rock equivalent of granite is rhyolite. Granite is nearly always massive and tough; these properties have made granite a widespread construction stone throughout human history. The average density of granite is between 2.65 and 2.75 g/cm3, its compressive strength lies above 200 MPa, its viscosity near STP is 3–6·1019 Pa·s. The melting temperature of dry granite at ambient pressure is 1215–1260 °C. Granite has poor primary permeability overall, but strong secondary permeability through cracks and fractures if they are present. Granite is classified according to the QAPF diagram for coarse grained plutonic rocks and is named according to the percentage of quartz, alkali feldspar and plagioclase feldspar on the A-Q-P half of the diagram.
True granite contains both alkali feldspars. When a granitoid is devoid or nearly devoid of plagioclase, the rock is referred to as alkali feldspar granite; when a granitoid contains less than 10% orthoclase, it is called tonalite. A granite containing both muscovite and biotite micas is called two-mica granite. Two-mica granites are high in potassium and low in plagioclase, are S-type granites or A-type granites. A worldwide average of the chemical composition of granite, by weight percent, based on 2485 analyses: Granite containing rock is distributed throughout the continental crust. Much of it was intruded during the Precambrian age. Outcrops of granite tend to form rounded massifs. Granites sometimes occur in circular depressions surrounded by a range of hills, formed by the metamorphic aureole or hornfels. Granite occurs as small, less than 100 km2 stock masses and in batholiths that are associated with orogenic mountain ranges. Small dikes of granitic composition called aplites are associated with the margins of granitic intrusions.
In some locations coarse-grained pegmatite masses occur with granite. Granite is more common in continental crust than in oceanic crust, they are crystallized from felsic melts which are less dense than mafic rocks and thus tend to ascend toward the surface. In contrast, mafic rocks, either basalts or gabbros, once metamorphosed at eclogite facies, tend to sink into the mantle beneath the Moho. Granitoids have crystallized from felsic magmas that have compositions near a eutectic point. Magmas are composed of minerals in variable abundances. Traditionally, magmatic minerals are crystallized from the melts that have separated from their parental rocks and thus are evolved because of igneous differentiation. If a granite has a cooling process, it has the potential to form larger crystals. There are peritectic and residual minerals in granitic magmas. Peritectic minerals are generated through peritectic reactions, whereas residual minerals are inherited from parental rocks. In either case, magmas will evolve to the eutectic for crystallization upon cooling.
Anatectic melts are produced by peritectic reactions, but they are much less evolved than magmatic melts because they have not separated from their parental rocks. The composition of anatectic melts may change toward the magmatic melts through high-degree fractional crystallization. Fractional crystallisation serves to reduce a melt in iron, titanium and sodium, enrich the melt in potassium and silicon – alkali feldspar and quartz, are two of the defining constituents of granite; this process operates regardless of the origin of parental magmas to granites, regardless of their chemistry. The composition and origin of any magma that differentiates into granite leave certain petrological evidence as to what the granite's parental rock was; the final texture and composition of a granite are distinctive as to its parental rock. For instance, a granite, derived from partial melting of meta
Baxter State Park
Baxter State Park is a large wilderness area permanently preserved as a state park, located in Northeast Piscataquis, Piscataquis County in north-central Maine, United States. It is in the North Maine Woods region, the Katahdin Woods and Waters National Monument borders Baxter State Park; the park was established by 28 donations of land, in trust, from park donor Percival P. Baxter between the years of 1931 and 1962 creating a park of over 200,000 acres in size. Baxter Park is not part of the Maine State Park system. Sole governance is provided by the Baxter State Park Authority, consisting of the Maine Attorney General, the Maine Commissioner of Inland Fisheries and Wildlife and the Director of the Maine Forest Service; the park is independently funded through a combination of revenues from trusts, user fees, the sale of forest products from the park's Scientific Forest Management Area. The park is home to Mount Katahdin; the number of visitors to the park declined from 75,000 in 2000 to 55,000 in 2005, but since 2005 visitor use has been increasing.
Mount Katahdin consists of a cluster of mountains. The highest peak, Baxter Peak, is named after park donor and former Maine Governor Percival P. Baxter and rises up to 5,267 feet; the mountain is the northern terminus of the Appalachian Trail. There are many bodies of water in the park; the three largest bodies of water are Grand Lake Matagamon, Webster Lake, Nesowadnehunk Lake. There are several smaller ponds, such as Hudson, Russell and the South Branch ponds. Numerous streams and rivers connect these water bodies, most prominently Trout Brook and Nesowadnehunk Stream; some of these have waterfalls. Wassataquoik Stream has two waterfalls and Norway. None of this water is potable, the park advises that visitors bring or treat their water; the climate of Baxter State Park lies within the Northern Forest Region of the American continent and experiences the cool, moist climate typical of this region. The annual mean temperature is 38.6 °F. The average annual precipitation is 37 inches. Summer temperatures and conditions peak in the park in August.
Leaf-fall in deciduous trees is complete by the end of October. Lasting snowfall begins in mid-to-late November, lasts through April. Leaves emerge on deciduous trees around the last week of May. Weather in Baxter State Park can be characterized by its variability. Baxter State Park has a diverse population of wildlife, the most common of which are the moose, the black bear, the white-tailed deer; these animals can sometimes be seen from the road. The many marshes and bogs of the park serve as habitats for such animals as beavers, river otters, raccoons. There are several active beaver colonies within the park's perimeters. Wooded areas of the park support other types of wildlife, including bobcats, martens, chipmunks, red squirrels, snowshoe hares, coyotes and red foxes. There is an avian population in the park; the park was a gift to the people of Maine from Governor Percival P. Baxter, who used his personal wealth over a 32-year period to purchase and donate the original 201,018 acres of the park starting with a 6,000 acres purchase in 1930 from the Great Northern Paper Company.
Since Gov. Baxter's death in 1969 the park has been increased to a total of 209,501 acres, including the 2006 addition of a parcel of 4,678 acres and spectacular Katahdin Lake. Park Headquarters is located over twenty miles from the actual park in the small town of Millinocket. There are no stores or gas stations inside the park. Access and use are regulated in accordance with Gov. Baxter's expressed desire to keep the park "forever wild." Baxter wrote of the area: "Man is born to die, his work short lived. Throughout the ages it will stand as an inspiration to the men and women of the state." In 1979, volunteers in the Maine Youth Conservation Corps created the mural on Pockwockamus Rock, located about a mile from the south gate. Inside the park boundary there is running water, or paved roads. In keeping with the "Forever Wild" philosophy expressed by Gov. Baxter, the park prohibits the use of audio or visual devices in any way that impairs the enjoyment of the park by others or that may disturb or harass wildlife.
Winter hiking and camping regulations have been revised to provide more freedom for park visitors, coupled with a clear understanding that park visitors must take responsibility for their safety in the unforgiving winter environment of the park. The park is open to overnight summer camping from May 15 to October 15 and winter camping from December 1 to March 31. Only northbound long distance Appalachian Tra