Belknap Crater is a shield volcano in the Cascade Range in the U.S. state of Oregon. Located in Linn County, it is associated with lava fields and numerous subfeatures including the Little Belknap and South Belknap volcanic cones. It lies north of McKenzie Pass and forms part of the Mount Washington Wilderness. Belknap is not forested and most of its lava flows are not vegetated, though there is some wildlife in the area around the volcano, as well as a number of tree molds formed by its eruptive activity.
Belknap was named for J. H. Belknap, whose father R. S. Belknap developed Belknap Springs. Early routes through the area extended near Belknap and its lava fields, and in the early 20th century, herds of sheep were moved to the two steptoes that lie among the Little Belknap lava flows to graze. The Oregon Skyline Trail, which runs to the west of Belknap's lava flows, follows paths used by Native American populations, who harvested huckleberries in the area. Today, there are a number of trails that run near Belknap, including ones that extend to Little Belknap and Belknap Crater. Belknap can be seen by tourists at the Dee Wright Observatory, which was built in-part with lava blocks from Belknap Crater.
A precise determination for Belknap's age has not been made, as its early history remains obscure. Belknap has likely been built up by eruptive activity over a long period of time. Belknap Crater has had four Holocene eruptive periods confirmed by geological evidence. In total, the Belknap shield and its multiple vents were formed in less than 1,500 years, its last eruptive episode finishing about 1,500 years ago. Belknap formed on the lower slopes of Mount Washington, a highly eroded volcano, and is one of the larger mafic (rich in magnesium and iron) volcanoes in the Sisters Reach.
Belknap consists of a shield volcano and pyroclastic cone and consists of basaltic and basaltic andesite lava with sub-alkaline composition, and it is characteristic of High Cascade volcanism. Well-preserved, its core is made of cinder materials; its eruptive deposits have well-preserved pressure ridges (tumuli) and levees. There are a number of subfeatures including the Inaccessible Cones, Little Belknap, South Belknap, and Twin Craters, as well as the Belknap hot springs. Postglacial, mafic eruptions are more common in the Sisters Reach — which includes Belknap — than anywhere in the Cascade volcanic arc. However, the Volcano Hazards Program of the United States Geological Survey considers it unlikely that Belknap will erupt again soon.
Hildreth (2007) lists Belknap Crater's summit elevation at 6,873 feet (2,095m).[5] McArthur and McArthur (1984) list its elevation at 6,877 feet (2,096m),[4] while according to the U.S. National Geodetic Survey, Belknap reaches an elevation of 6,876 feet (2,096m), and has a "bald" appearance.[1] The central Belknap shield volcano has a diameter of 5 miles (8.0km)[2] and a volume of 2.4 cubic miles (10km3),[5][a] with a maximum thickness of 1,700 feet (520m).[6] The shield has proximal and draping reliefs of 1,362 and 4,429 feet (415 and 1,350m), which are the "difference between summit elevation and that of highest exposure of older rocks overlain by the edifice" and the "difference between summit elevation and that of lowest distal lavas of the edifice (not including distal pyroclastic or debris flows)," respectively.[5] According to Hildreth (2007), Belknap Crater is a broad, low-angled shield volcano compared to other mafic (rich in magnesium and iron) volcanic cones.[7] Belknap's summit cone rises about 400 feet (120m) above the base shield volcano,[8] and the volcano itself rises about 1,600 feet (490m) above its surroundings.[9]
Oregon Route 242, which follows the course of the McKenzie River, passes through the lava fields produced by Belknap Crater, the Yapoah cinder cone volcano, and a number of other volcanic vents. These fields consist of black, basaltic lava and encompass an area of 85 square miles (220km2).[10]
Ecology
Small stands of trees near Belknap Crater
Belknap forms part of the Mount Washington Wilderness, which encompasses 54,278 acres (219.66km2) of lava and plains. Lodgepole pine trees are common, and there are 28 lakes within the wilderness area.[11] Belknap itself is not forested and its lava flows are generally not vegetated,[12] though there were trees growing on its lava flow deposits in the 1960s according to Taylor (1965).[13] He observed only sparse growth of trees on lava flows from Little Belknap in a report published in the 1980s, noting that soil from Belknap was about 3-foot (0.91m) thick and made up of lapilli and volcanic ash, which came mostly from Belknap Crater.[14] Along the trail to Little Belknap Crater, there is a tree island with lodgepole pine, mountain hemlock, and true fir.[15] There are also ground squirrels running around on lava flows from Belknap.[15] Along the Oregon Skyline Trail, which passes west of Belknap, there are black-tailed and mule deer as well as lakes stocked with Eastern brook trout[16]
Along the western flows produced by Belknap, there are several dozen tree molds, which range from 1 to 5 feet (0.30 to 1.52m) in diameter and 6 to 15 feet (1.8 to 4.6m) in depth. Some fell into the lava, forming hemi-cylinder-shaped trenches up to 35 feet (11m) in length. Taylor (1965) identified a system of radial roots that were charred from the lava under soil at one of the molds. The material underwent radiocarbon dating to determine an age of 360 ± 160 years A.D.[17]
Geology
Belknap formed on the lower slopes of Mount Washington (seen on the right)Belknap viewed from space in 1973
The Cascade Range resulted from the subduction of the Juan de Fuca tectonic plate under the North American tectonic plate, with the High Cascade subprovince in central Oregon forming about 160 to 190 miles (250 to 300km) east of the margin of convergence.[18] The High Cascade platform of the Cascade Volcanic Arc consists of overlapping layers of lava flows produced by shield volcanoes within the past 2 million years. The Cascade shields are steeper and smaller than Hawaiian shield volcanoes, often featuring cinder cones at their summit.[19]
Belknap is the youngest shield volcano in the Cascade arc by far,[19] with rugged, barren lava fields that contrast with the forested fields of older Cascade shields.[19][20] It lies within the central Oregon segment of the Cascades near the Three Sisters area, which is marked by closely clustered volcanic centers that include, from south to north, Mount Bachelor, the Three Sisters, and Belknap.[21]
Known as the Sisters Reach,[22] the cluster abruptly broadens first to a width of 22 miles (35km) then to 28 miles (45km) as it approaches its southern end, running for about 56 miles (90km) in length. There are at least 466 Quaternary volcanoes in the Sisters Reach, including several aligned segments of volcanic vents and rare eruptive units of rhyolite (uncommon elsewhere in the Cascade arc).[22] Between the North Sister and Three Fingered Jack volcanoes, Holocene volcanism has been intense, with at least 125 volcanic centers becoming active between 4,000 and 1,300 years ago.[23] Belknap was the last volcano to erupt in the Three Sisters area.[21] Basaltic andesite dominates the eruptive material in the local mafic volcanoes, which range from early Pleistocene to Holocene age.[22]
Belknap is one of the larger mafic volcanoes in the Sisters Reach, more than 30 of which run continuously along the segment.[22] As with other mafic volcanic fields in and next to the Cascades, it does not exhibit a distinct pattern for compositional evolution over time like at the Hawaii hotspot.[24] The area by Belknap and Mount Bachelor is marked by extensional tectonics, with a high density of mafic (rich in magnesium and iron) volcanic vents.[24] There are clear trends among volcanic centers in the area including at Sand Mountain and Inaccessible Cone, suggesting underlying faults; according to Taylor (1965), Belknap's alignment with the Spatter Cone Chain and Blue Lake Crater might similarly indicate underlying faults or fractures connecting the vents at depth, though there are some irregularities. One important distinction is that almost all vent patterns in the area except the supposed Belknap–Blue Lake alignment individually trend north–south, no matter the alignment of the aggregate trend.[25]
Belknap formed on the lower slopes of Mount Washington, a highly eroded volcano;[10] Mount Washington's pinnacle lies about 3 miles (4.8km) from Belknap.[26]Dissolved magmatic carbon dioxide flux at Mount Washington and Belknap Crater was calculated by James et al. (1999) to be 5.3 pounds (2.4kg) per year.[27] Belknap consists of a shield volcano[28] and pyroclastic cone,[3] which form a late Holocene shield volcano complex.[2] It is made up of basaltic and basaltic andesite lava,[3] which is sub-alkaline.[28] Mafic in composition,[2][5] it is characteristic of High Cascade volcanism. In addition to its shield volcano vents, the Belknap complex also consists of lava flows and tephra deposits erupted from one central vent and several other flank vents. Its lava flows encompass about 39 square miles (100km2).[2] It has a pyroclastic core.[20] The more southern of the two craters on Belknap's summit cone has a depth of 250 feet (76m) and width of more than 1,000 feet (300m) at its rim.[29]
Belknap is one of three major lava fields in its area with Sand Mountain and Yapoah–Four-in-One–Collier. Of these, Belknap is the largest, encompassing Belknap Crater's shield, Little Belknap, and South Belknap cone. Lava flows in the area have a black and glassy appearance with a vesicular texture.[30] The basalt and basaltic andesite lava flows from Belknap include small plagioclase and olivine phenocrysts, which run for 0.039 inches (1mm) across, as well as glomerocrysts, which are sparse and run up to 0.28 inches (7mm) across. Some of the lava flows encased charcoal.[12] Lava flows range from olivine basalt to basaltic andesite and generally show few signs of weathering or mineral alteration, with solid cores and outer surfaces with jagged volcanic blocks and flow breccia. The cores of lava deposits are inaccessible, except at lava tubes, lava gutters, road cuts, and quarries.[30]
Belknap is well-preserved and serves as a good example of Holocene-era activity in the High Cascades. Its core consists of cinder, which is surrounded by a broad shield. It marks an intermediate scale between cinder cones that produced small lava flows such as Twin Craters or Yapoah and larger volcanoes like Mount Washington or Three Fingered Jack.[28] Along with lava flows from the Sand Mountain Volcanic field and other young volcanic centers in the Santiam and McKenzie Pass area,[12] many of the lavas produced by Belknap have crusts with slag or volcanic blocks, with a smaller number having surfaces with ropy, pāhoehoe appearances.[12][31] The deposits consist of piles of basaltic andesite shards arranged in piles as a result of collapsed lava tubes and breakage of lava crusts and interior lava flows that continued moving while their exteriors cooled;[31] Taylor (1965) wrote that Belknap "is only a pile of cinders on the summit of a vast shield of recent lava."[13] The estimated volume of cinders at Belknap Crater is 75,000,000 cubic yards (57,000,000m3).[32]
Belknap's volcanic deposits have well-preserved pressure ridges (tumuli) and levees on their surfaces, and they were emplaced between 7,000 and 1,300 years ago.[12] Tephra erupted from Sand Mountain Volcanic Field and Belknap forms a thick blanket across Santiam Pass and near McKEnzie Pass, with radiocarbon dating ages of 3,440 ± 250 to 1,600 years B.P. for deposits from source vents, making them younger than Mazama Ash deposits.[33] Cinder cones near Inaccessible Cone have been nearly buried to completion by basalt and basaltic andesite erupted from Belknap.[33] Belknap's ash deposits are recognizable by their dark color among road cuts and at near the base of lava flow margins.[34]
Little Belknap shield, formed about 3,000 years ago, sits to the right of a 490-foot (150m) high scoria cone of the main Belknap Crater vent, with Mount Washington located to the right of both cones.[37] It is about 1 mile (1.6km) east of Belknap shield's summit craters.[38] Erupted on the flank of the much more extensive Belknap Crater, which also has its own secondary eruptive vents, Little Belknap lacks scoria cones, potentially because it was fed by magma that was degassed prior to its eruption.[37]
Eruptions at Little Belknap were "quiet",[38] but voluminous, creating the separate shield, which is topped with cinders and lava blocks with collapsed lava tubes radiating outward. A western tube forms a confluence with a vertical conduit that has a diameter of about 20 feet (6.1m). Little Belknap's lava flows extended to within 1 mile (1.6km) of Windy Point to the east and McKenzie Pass to the southeast, forming deposits over ash from Belknap Crater and covered by lava flows from Yapoah Cone.[38] Along the Skyline Trail, one of the lava flows from Little Belknap peeled back on itself as it cooled, creating overturned slabs of hardened lava with widths up to 10 feet (3.0m) and lengths up to 50 feet (15m). The blocks are often parallel to the lava's flow direction; Taylor (1965) called them "lava curls".[38]
There is a small lava cave system near the summit of Little Belknap, which has spatter material for a roof. The cave system is short with a number of lava tubes. At the bottom of the conduit lies another system of lava tubes, which served as a drain to create a lava tube system with two levels that are connected by this open conduit, which C. E. Skinner (1982) calls "quite unusual."[39] The open vertical conduit cave has a diameter of 20 feet (6.1m), dropping 24 feet (7.3m) between the upper and lower cave systems. It has an ovular shape and a remelted lining with stalactites made from lava.[40]
South Belknap is a small volcano 1 mile (1.6km) to the south of Belknap, which was breached on its southwestern side by lava flows that also extended over Belknap Crater's southern base. Early lava flows near South Belknap were covered by a later lava flow, which was produced by a vent located about 300 feet (91m) northwestward.[17] This lava flow also overlapped with the western part of Belknap Crater's lava, and then it reached Lake Valley, where it formed the northern shore of the local Hand Lake.[41] A deposit of alluvium abuts the margin of South Belknap's lava deposits.[34]
On top of Belknap Crater, there is a 400-foot (120m) high cinder cone, which may be the surface extension of the inner pyroclastic core.[20] Within it are three craters, all of different size, which align along a north–northwestern trend. The southern crater is large and produced most of the tephra that covers the surrounding area; the northernmost crater is smaller and erupted ash and a lava flow, which breached the rim of the crater.[31] The Little Belknap volcano erupted lava flows that formed steptoes out of two hills by surrounding them with black, basalt. Its most recent eruptions filled its crater and created a mound of red rock with clinkers; there are a number of collapsed lava tubes diverging radially from the crater.[31]
Besides the volcanic vents related to Belknap Crater, there are two volcanoes south of Belknap which were also recently active: Four-in-One Cone and Collier Cone.[31] Another, unnamed cone at the northern end of Inaccessible Cone's alignment, which rises to a height of 300 feet (91m), was breached on its western and southwestern sides by gray basalt lava, which is older than Sand Mountain Volcanic Field and Belknap.[42] There may have been a large lava field in the glacier valley north of the Twin Craters cone, but any evidence is now buried under the Belknap shield.[8] There is a glaciated steptoe (island) in the western part of the Belknap lava field.[43] Deposits from Belknap buried older lava flows from the Sand Mountain Volcanic Field[44] as well as a series of four cinder cones located about 3.5 miles (5.6km) to the southwest of Mount Washington.[42] There are also deposits from Belknap in the Lake Valley region between Belknap and both Sims Butte and Mount Mazama.[34]
There are hot springs, known as the Belknap Hot Springs, on the northern bank of the McKenzie River.[45] Located in Lane County, they were discovered by R. S. Belknap in November 1869.[4] They lie 4 miles (6.4km) to the southwest of the wilderness area, ejecting water at a rate of 75 U.S. gallons (280L) per minute with a temperature of 180°F (82°C).[46] The hot springs are indicative of a fault that underlies the Cascade Volcanoes, onto which the east side dropped down and lava intrusions formed volcanic centers.[47]
Eruptive history
Eruptions at Belknap Crater built up the main shield volcano over repeated activity from vents surrounding a composite summit cone. The lava had a fluid character, leading to inundation of an area that encompassed more than 37 square miles (96km2). Rather than forming extensive streams, the lava settled into shorter channels that intersected, leaving complicated drainage patterns. The volcano sits on top of the thick and extensive lava deposits left behind.[8] Belknap Crater has been the focal point for Holocene volcanism producing basaltic and basaltic andesitic lava in its vicinity, which was complex and sustained over a long period of time.[6]
According to the Global Volcanism Program, Belknap Crater had four Holocene eruptive periods confirmed by geological evidence including corrected radiocarbon dating and magnetism; their durations are not known.[b] The first took place in 5050 BCE, producing the Tamolitch lava flow. The next eruptive event, which took place in 1030 BCE ± 300 years, had a VEI of 0 and took place at Little Belknap. The subsequent eruption at South Belknap and Twin Craters occurred in 800 BCE ± 300 years and had a VEI of 2 (Strombolian/Vulcanian); it was followed by the most recent identified event at Belknap Crater in 480, which also had a VEI of 2. According to the Global Volcanism Program, these four eruptions took place during the Holocene:[3]
A precise determination for Belknap's age has not been made,[48] as its early history remains obscure,[12] though it is likely that Belknap has been built up by eruptive activity over a long period of time.[12][48] Belknap's oldest exposed lava deposits are located on the eastern flanks of the volcano, produced by vents that may have been buried by later activity. They coursed mostly to the northeast and split into two lobes on both sides of the Dugout Butte ridge, extending about 7 miles (11km) from their source vent,[8] along the eastern edges of the Deschutes National Forest.[49]
Between 3,000 and 1,500 years ago during the late Holocene epoch, the Belknap shield volcano as well as the Belknap Crater cone and Little Belknap shield volcano erupted, generating lava flows that spread throughout the McKenzie Pass area. Belknap Crater's lava flows were produced from its northeastern base and extended 9.3 miles (15km) to the west, reaching the McKenzie River valley. These events represent one of the largest periods of recent volcanism in the Cascade Range,[3] and were comparable in terms of effusion rates to the formation of Mount Bachelor.[50]
The initial eruptions generated tephra, which covered an extensive area to the northeast and southeast, as well as basaltic lava flows that extended 6 miles (9.7km) from the burgeoning shield volcano edifice[2] to the east.[28] Thin scoria deposits occur west of Belknap; on the eastern slopes, lava deposits are covered with black ash and fine cinders. There is also an ash blanketing an expansive area from Dry Creek to the north to Black Crater to the south, with ash deposits as far as 8 miles (13km) eastward.[17] These eruptions were produced from two, deep craters on top of Belknap's cone, forming lapilli tuff on their eastern rim walls.[8] There are also thick rocks in the walls of the more southern crater,[29] as well as some lava that breached the southwestern rim, which has been obscured by spatter. The northern crater contains spindle volcanic bombs at its western rim, which reach up to 3 feet (0.91m) in length. A broad pit formed at the northern base of Belknap's cone, running for 200 feet (61m) in length, and was likely blasted through a bocca.[17] According to Taylor (1965), a strong prevailing wind moving east influenced the distribution of ash and cinders on Belknap's rim.[17]
Eruptions during a subsequent phase about 2,900 years ago built a smaller shield volcano, Little Belknap.[2] According to Sherrod et al. (2004), lava from Little Belknap formed a tree mold in the southern part of the Sand Mountain volcanic field, which was dated to 2,883 ± 175 years Before Present (B.P.) via radiocarbon dating.[48] Sherrod et al. (2004) also describe charcoal detected under a lava flow that coursed down Belknap Crater's western flank, which yielded two radiocarbon dating ages: 1,590 ± 160 years B.P. and 1,400 ± 100 years B.P. These ages have overlap at the level of statistical certainty, indicating that they could have been erupted nearly simultaneously or as far apart as 800 years. Both flows came from the shield volcano's summit vent. Early lava flows at Belknap were erupted from actively erupting volcanic vents before Little Belknap formed, as demonstrated by stratigraphy.[51]
A third eruptive period constructed the bulk of the volcanic complex[28] with basaltic andesite lava from Belknap Crater's central vent about 1,500 years ago. This cone-building phase was also fed by eruptions about 1,700 years ago at a vent about 1 mile (1.6km) to the south, South Belknap.[2] According to Sherrod et al. (2004), South Belknap formed charred roots at a tree mold with a radiocarbon dating age of 2,635 ± 50 years B.P., the same site that Taylor used to determine an age of 1,775 ± 400 years B.P.[12] Taylor also argues that the cone was breached about 1,800 years ago before it was surrounded by basaltic andesite lava flows from another vent about 1,500 years ago.[6] Sherrod et al. argue that the older date (2,635 ± 50 years B.P.) is more accurate because the deposit contains concentrated amounts of the cosmogenic nuclideisotope3He, which would require a longer surface exposure than Taylor's calculation would allow,[48] at least 2,000 years B.P.[12]
A final eruptive phase produced lava flows that extended 9 miles (14km) to the west into the McKenzie River valley,[2] also coursing to the north and south.[17] These lava deposits have ropy surfaces and feature squeeze-ups between broken platforms of crust. The lava that moved south crossed over more ancient lava from Twin Craters, while the lava that ran to the west covered lava and cinder cones within the Inaccessible Cone lineament. The west-moving lavas also moved over Sand Mountain lava flows (erupted from the southern group of vents and the southern vent of Sand Mountain itself), entering the McKenzie Canyon.[17] The lava from this eruption significantly influenced the McKenzie River, creating the upstream swamp known as Beaver Marsh, with the remnants of these lava streams now forming permeable sediment talus for the McKenzie River, which disappears into them before re-emerging at Tamolitch Falls.[17] Erosion has altered the area downstream from these falls to a lateral terrace on the wall of the McKenzie Canyon, 30 feet (9.1m) above the river water level.[17]
In total, the Belknap shield and its multiple vents were formed in less than 1,500 years, which was a comparable effusion rate to the Nash Crater scoria cone, the Sand Mountain Volcanic Field, and the Mount Bachelor chain.[52] Eruption rates for Belknap were high,[53] at 1.2 cubic miles (5km3) per 1,000 years,[54] similar to the buildup of rhyodacite before the climactic eruption at Mount Mazama.[53] Within the last 15,000 years, Cascades volcanoes have erupted about 70 cubic miles (290km3) of material excluding rear-arc volcanoes. Of this, about 15 cubic miles (61km3) (21 percent) came from 63 distributed or peripheral cones, shields, or mafic and intermediate composition chains, with Belknap and Mount Bachelor contributing 71 percent of that material.[53] Over the course of its eruptive history, Belknap erupted 1.4 to 2.2 cubic miles (6 to 9km3) of material with several eruptive pulses.[54]
Recent activity and potential hazards
Postglacial, mafic eruptions are more common in the Sisters Reach — which includes Belknap — than anywhere in the Cascade volcanic arc.[22] A lava flow lies next to South Cinder Peak, the Nash Crater–Lost Lake cone cluster, Sand Mountain Volcanic Field, Inaccessible Cone chain, Blue Lake Crater, and a number of monogenetic scoria cones and chains.[22] The McKenzie and Santiam Pass area saw more than a dozen distinct mafic eruptions between 4,500 and 1,100 years ago according to radiocarbon dating, which corresponded to a pulse of mafic eruptions in the late Holocene epoch. Other nearby mafic eruptive units occur at Sims Butte, Cayuse Crater, LeConte Crater, Mount Bachelor, the Egan Cone cluster, and the Katsuk-Talapus chain, which likely were all emplaced between 18,000 and 8,000 years ago.[22] At the south of Sisters Reach, there is a postglacial, basalt lava flow that lies on the eastern flank of Sitkum Butte (a cone that is older than this lava flow).[22] The recent eruptive activity at Belknap Crater means that it is one of the youngest mafic volcanoes in the Oregon Cascades.[55]
There are about 6,500 people living within 19 miles (30km) of Belknap Crater, with a population of about 362,000 within 62 miles (100km).[3] However, most eruption hazards from basaltic volcanoes are generally restricted to within 9.3 miles (15km) of the vent, with some exceptions.[56] According to the Volcano Hazards Program of the United States Geological Survey's Cascades Volcano Observatory, the threat potential from Belknap is "Low/Very Low".[2] It does not seem likely that Belknap Crater will erupt again, though eruptions with similar characteristics to its past eruptions might occur in the surrounding area, disrupting transportation on major highways in the vicinity including U.S. Route 20, Oregon Route 22, and Oregon Route 242. The eruption of tephra could pose a threat to surrounding communities, particularly within central Oregon to the east.[2] High-volume lahars (mudflows or debris flows composed of a mix of pyroclastic material, rocky debris, and water) would travel far to the west. Moreover, low-volume lahars from eruptions would likely enter the McKenzie River valley, which is broad and fairly gently sloped, where they might move downstream through flood plains or small channels. Near Belknap Springs and McKenzie Bridge, deposits from the eruption could also block off water upstream, leading to downstream lahars and floods.[57]
Human history
Belknap was named for J. H. Belknap, who lived along the McKenzie River and was the son of R. S. Belknap, responsible for developing Belknap Springs. J. H. Belknap had an interest in the toll road constructed over McKenzie Pass during the early 1870s.[4] The Belknap family came to the state of Oregon in 1847 with the Orem family, followed by G. Belknap and J. Belknap in 1848. The Belknap Springs in Lane County were found by R. S. Belknap in November 1869 and developed them, and he became the postmaster for the Salt Springs post office, which was established in October 1874. The name for the Salt Springs office changed to Belknaps Springs in June 1875, then Belknap Springs in 1891.[4]
During the days of the American pioneer, the Santiam and McKenzie passes were the two major routes through the Deschutes Forest area, eventually transforming into highways for Oregon's interior. The Willamette Pass to the south was used as a route by travelers as early as 1853, noting its difficult as the "route was far from a road."[58] Still, the road was heavily used in spite of its poor conditions, later becoming the Willamette Pass Highway, better known as Oregon Route 58.[58] In 1862, the Scott brothers and colleagues formed the McKenzie Fork Wagon Road Company to create a better road passing over lava fields in the area, then later the McKenzie River Wagon Road Company, which had as its objective a road that crossed the Cascade Range near the Three Sisters volcano complex at the Deschutes River. A third group followed that aimed to forge a road across the Deschutes north of the Sisters. The original route pursued by the Scott brothers reached the Belknap hot springs.[59]
In the early 20th century, herds of sheep were moved to the two steptoes that lie among the Little Belknap lava flows to graze.[60] The Oregon Skyline Trail, which runs to the west of Belknap's lava flows, follows paths used by Native American populations, who harvested huckleberries in the area.[16]
Recreation
Belknap as seen from the Dee Wright Observatory
The Dee Wright Observatory was built with lava blocks from the lava fields produced by Belknap, Yapoah cinder cone, and other volcanoes. It offers views of local volcanoes; Belknap lies to the north.[10] Both Belknap Crater and Little Belknap Crater can be reached from spurs of the Pacific Crest Trail. The round trip from intersection of the Pacific Crest Trail and Oregon Route 242 to Little Belknap Crater is about 5.6 miles (9.0km) and ranges in elevation from 5,350 to 6,250 feet (1,630 to 1,900m), with an easy to moderate difficulty level.[61] The round trip to Belknap Crater is about 6.8 miles (10.9km) from the trailhead and is more difficult owing to the steep climb to the summit on fine cinders.[61]
The trail offers views of nearby Mount Washington,[62] Black Crater, and the Three Sisters,[63] as well as lava features.[62] Trees and other forms of wildlife are rare along the trail.[64] There is also a trail that extends to Belknap Crater, which runs about 6.8 miles (10.9km) round trip, with an intermediate difficulty level. It can also be skied.[65] The Oregon Skyline Trail, part of which runs for 38 miles (61km) through the Deschutes National Forest, passes westward of the Belknap lava fields. It has been recognized as a major scenic route since 1920.[16]
Notes
[a] ^ This volume comes from Hildreth (2007); Taylor (1981) estimated its volume to be 1.3 cubic miles (5.4km3).[6]
[b] ^ Taylor (1990) lists three principal eruptive episodes between about 3,000 and 1,500 years Before Present (BP). However, he still lists the four eruptions that the Cascades Volcano Observatory and Global Volcanism Program describe;[2][3][28] he considers the two most recent eruptions to be part of the third major eruptive phase.[28]
[c] ^ Sherrod et al. (2004) disagree with this date for the eruptive phase at South Belknap. As mentioned in the text, Sherrod et al. calculated a radiocarbon dating age of 2,635 ± 50 years B.P. for the same site that Taylor used to generate this estimated age, which is equivalent to 1,775 ± 400 years B.P.[48]
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Newberry Volcano is a large, active, shield-shaped stratovolcano located about 20 miles (32 km) south of Bend, Oregon, United States, 35 miles (56 km) east of the major crest of the Cascade Range, within the Newberry National Volcanic Monument. Its highest point is Paulina Peak. Newberry is the largest volcano in the Cascade Volcanic Arc, with an area of 1,200 square miles (3,100 km2) when its lava flows are taken into account. From north to south, the volcano has a length of 75 miles (121 km), with a width of 27 miles (43 km) and a total volume of approximately 120 cubic miles (500 km3). It was named for the geologist and surgeon John Strong Newberry, who explored central Oregon for the Pacific Railroad Surveys in 1855.
Mount Jefferson is a stratovolcano in the Cascade Volcanic Arc, part of the Cascade Range in the U.S. state of Oregon. The second highest mountain in Oregon, it is situated within Linn County, Jefferson County, and Marion County and forms part of the Mount Jefferson Wilderness. Due to the ruggedness of its surroundings, the mountain is one of the hardest volcanoes to reach in the Cascades. It is also a popular tourist destination despite its remoteness, with recreational activities including hiking, backpacking, mountaineering, and photography. Vegetation at Mount Jefferson is dominated by Douglas fir, silver fir, mountain hemlock, ponderosa pine, lodgepole pine, and several cedar species. Carnivores, insectivores, bats, rodents, deer, birds, and various other species inhabit the area.
Mount Mazama is a complex volcano in the western U.S. state of Oregon, in a segment of the Cascade Volcanic Arc and Cascade Range. The volcano is in Klamath County, in the southern Cascades, 60 miles (97 km) north of the Oregon–California border and. Its collapse, due to the eruption of magma emptying the underlying magma chamber, formed a caldera that holds Crater Lake. Mount Mazama originally had an elevation of 12,000 feet (3,700 m), but following its climactic eruption this was reduced to 8,157 feet (2,486 m). Crater Lake is 1,943 feet (592 m) deep, the deepest freshwater body in the U.S. and the second deepest in North America after Great Slave Lake in Canada.
Three Fingered Jack is a summit of a shield volcano of the Cascade Range in the U.S. state of Oregon. Formed during the Pleistocene epoch, the mountain consists mainly of basaltic andesite lava and was heavily glaciated in the past. While other Oregon volcanoes that were heavily glaciated—such as Mount Washington and Mount Thielsen—display eroded volcanic necks, Three Fingered Jack's present summit is a comparatively narrow ridge of loose tephra supported by a dike only 10 feet (3.0 m) thick on a generally north–south axis. Glaciation exposed radiating dikes and plugs that support this summit. The volcano has long been inactive and is highly eroded.
Mount Washington is a deeply eroded volcano in the Cascade Range of Oregon. It lies within Deschutes and Linn counties and is surrounded by the Mount Washington Wilderness area.
Indian Heaven is a volcanic field in Skamania County in the state of Washington, in the United States. Midway between Mount St. Helens and Mount Adams, the field dates from the Pleistocene to the early Holocene epoch. It trends north to south and is dominated by six small shield volcanoes; these shields are topped by small spatter and cinder cones, and the field includes a number of subglacial volcanoes and tuyas. The northernmost peak in the field is Sawtooth Mountain and the southernmost is Red Mountain; its highest point is Lemei Rock at an elevation of 5,925 feet (1,806 m).
Broken Top is a glacially eroded complex stratovolcano. It lies in the Cascade Volcanic Arc, part of the extensive Cascade Range in the U.S. state of Oregon. Located southeast of the Three Sisters peaks, the volcano, residing within the Three Sisters Wilderness, is 20 miles (32 km) west of Bend, Oregon in Deschutes County. Eruptive activity stopped roughly 100,000 years ago, and erosion by glaciers has since reduced the volcano's cone to where its contents are exposed. There are two named glaciers on the peak, Bend and Crook Glacier.
The Boring Lava Field is a Plio-Pleistocene volcanic field with cinder cones, small shield volcanoes, and lava flows in the northern Willamette Valley of the U.S. state of Oregon and adjacent southwest Washington. The field got its name from the town of Boring, Oregon, located 12 miles (20 km) southeast of downtown Portland. Boring lies southeast of the densest cluster of lava vents. The zone became volcanically active about 2.7million years ago, with long periods of eruptive activity interspersed with quiescence. Its last eruptions took place about 57,000 years ago at the Beacon Rock cinder cone volcano; the individual volcanic vents of the field are considered extinct, but the field itself is not.
The Three Sisters are closely spaced volcanic peaks in the U.S. state of Oregon. They are part of the Cascade Volcanic Arc, a segment of the Cascade Range in western North America extending from southern British Columbia through Washington and Oregon to Northern California. Each over 10,000 feet in elevation, they are the third-, fourth- and fifth-highest peaks in Oregon. Located in the Three Sisters Wilderness at the boundary of Lane and Deschutes counties and the Willamette and Deschutes national forests, they are about 10 miles south of the nearest town, Sisters. Diverse species of flora and fauna inhabit the area, which is subject to frequent snowfall, occasional rain, and extreme temperature variation between seasons. The mountains, particularly South Sister, are popular destinations for climbing and scrambling.
Black Butte is an extinct stratovolcano in the U.S. state of Oregon. Located in Jefferson County, it is part of Deschutes National Forest. Black Butte forms part of the Cascade volcanic arc. The butte lies just south of the Metolius Springs, which merge to form the headwaters of the Metolius River. The Metolius River's basin sustains a wide array of plant life, large and small mammals, and more than 80 bird species.
Diamond Peak is a volcano in Klamath and Lane counties of central Oregon in the United States. It is a shield volcano, though it might also be considered a modest stratocone. Diamond Peak forms part of the Cascade Volcanic Arc, a segment of the Cascade Range in western North America extending from southern British Columbia through Oregon to Northern California. Reaching an elevation of 8,748 feet (2,666 m), the mountain is located near Willamette Pass in the Diamond Peak Wilderness within the Deschutes and Willamette national forests. Surrounded by coniferous forest and visible in the skyline from foothills near Eugene, Diamond Peak offers a few climbing routes and can be scrambled. Diamond Peak is one of Oregon's Matterhorns.
Olallie Butte is a steep-sided shield volcano in the Cascade Range of the northern part of the U.S. state of Oregon. It is the largest volcano and highest point in the 50-mile (80 km) distance between Mount Hood and Mount Jefferson. Located just outside the Olallie Scenic Area, it is surrounded by more than 200 lakes and ponds fed by runoff, precipitation, and underground seepage, which are popular spots for fishing, boating, and swimming. The butte forms a prominent feature in the Mount Jefferson region and is usually covered with snow during the winter and spring seasons.
Hoodoo Butte is a cinder cone butte in the Cascade Range of northern Oregon, located near Santiam Pass. Immediately to the east lies Hayrick Butte, a prime example of a tuya; the two mountains' names were likely mistaken for each other, but stuck with them over time. The area has been subjected to a number of historic fires. Hoodoo is sometimes considered a subfeature of the Mount Washington shield volcano, and it forms part of the Sisters Reach, which extends from South Cinder Peak to Crane Prairie Reservoir, running for 56 miles (90 km). This region has a high vent density, with many mafic volcanoes of Pleistocene to Holocene age, such as Hoodoo. While Hoodoo has an intact summit crater that was blocked from erosion by glaciers, it has an irregular topography, giving it an open appearance.
Hayrick Butte is a tuya, a type of subglacial volcano, in Linn County, Oregon. Located in the Willamette National Forest near Santiam Pass, it lies adjacent to the cinder cone Hoodoo Butte, which has a ski area. Hayrick Butte likely formed when lava erupted underneath an overlying glacier or ice sheet, producing the flat top with near-vertical walls along the ice-contact margin as the lava cooled and hardened. Hayrick Butte has a nearly flat plateau about 0.5 miles (0.80 km) across and steep walls rising about 700 feet (0.21 km) above its surroundings. A cartographer accidentally switched the names for nearby Hoodoo Butte and Hayrick Butte; the word "hoodoo" usually refers to rock piles and pinnacles like those observed at Hayrick Butte.
Black Crater is a shield volcano in the Western Cascades in Deschutes County, Oregon. Located near McKenzie Pass, the volcano has a broad conical shape with gentle slopes. The volcano likely formed during the Pleistocene and has not been active within the last 50,000 years. Eruptive activity at the volcano produced mafic lava flows made of basaltic andesite and olivine basalt; it also formed a number of cinder cones. A normal fault occurs on the western side of the volcano, trending north–south. The volcano has been eroded by glaciers, which carved a large cirque into the northeastern flank of the mountain, forming its current crater.
Pelican Butte is a steep-sided shield volcano in the Cascade Range of southern Oregon. It is located 28 miles (45 km) due south of Crater Lake and 12 miles (19 km) northeast of Mount McLoughlin. Ice age glaciers carved a large cirque into the northeast flank of the mountain. Several proposals have been made over the last few decades for ski area development on the northeast flanks of the volcano, but there are no current plans to develop a ski area on the mountain.
Blue Lake Crater is a maar, or a broad, low-relief volcanic crater, in the U.S. state of Oregon. Located in Jefferson County, it consists of three overlapping craters, which hold Blue Lake. The drainage basin for Blue Lake has very steep, forested slopes and is mostly part of the explosion crater left by the volcano's eruption. The volcano lies within the Metolius River basin, which supports a wide array of plant life, large and small mammals, and more than 80 bird species. A 2009 Oregon law designated the Metolius River basin as an area of critical concern, preventing large-scale development and protecting wildlife.
Trout Creek Hill is a small Pleistocene basaltic shield volcano in Washington, United States. Located in Skamania County, Trout Creek Hill rises to an elevation of 2,946 feet (898 m). It is part of the Cascade Volcanic Arc, located in the Marble Mountain-Trout Creek Hill volcanic field.
The Sand Mountain Volcanic Field is a volcanic field in the upper McKenzie River watershed, located in the United States in Oregon. Part of the Cascade Volcanic Arc, it lies southwest of Mount Jefferson and northwest of Belknap Crater and Mount Washington. Its highest elevation is 5,463 feet (1,665 m).
Taylor, E. M.; Causey, J. D. (1984), "Mount Washington Wilderness, Oregon", in Marsh, S. P.; Kropschot, S. J.; Dickinson, R. G. (eds.), Wilderness Mineral Potential: Assessment of Mineral-Resource Potential in U.S. Forest Service Lands Studied 1964-1984, United States Geological Survey, pp.893–895, doi:10.3133/pp1300, Geological Survey Professional Paper Issue 1300, Volume 2.
Williams, I. A. (May 1916). "Some little-known scenic pleasure places in the Cascade Range in Oregon". Mineral Resources of Oregon. 2. Oregon Bureau of Mines and Geology.
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