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Newberry Volcano
Newberry Volcano
Newberry Volcano
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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.

Key Information

The volcano contains a large caldera, 4 by 5 miles (6.4 km × 8.0 km) in diameter, known as the Newberry Caldera. Within the caldera are two lakes: Paulina Lake and East Lake. The volcano and its vicinity include many pyroclastic cones, lava flows and lava domes; Newberry has more than 400 vents, the most of any volcano in the contiguous United States. Glaciers may have once been present at the volcano, though this remains contested. The area has a dry climate with low precipitation levels and little surface runoff.

The origin of the volcano remains somewhat unclear; while some scientists believe it originated from an independent hotspot, most evidence indicates that it formed from the subduction of the oceanic Juan de Fuca and Gorda tectonic plates under the continental North American Plate. Eruptive activity at Newberry Volcano began about 600,000 years ago and has continued into the Holocene, the last eruption taking place 1,300 years ago. Unlike other shield-shaped volcanoes, which often erupt basaltic lavas only, Newberry Volcano has also erupted andesitic and rhyolitic lavas. A popular destination for hiking, fishing, boating, and other recreational activities, the volcano lies within 19 miles (31 km) of 16,400 people and within 62 miles (100 km) of nearly 200,000 people, and it continues to pose a threat to life. Still considered an active volcano, it could erupt and produce lava flows, pyroclastic flows, lahars (volcanically induced mudslides, landslides, and debris flows), ashfall, earthquakes, avalanches, and floods. To track this threat, the volcano and its surroundings are closely monitored with sensors by the United States Geological Survey.

Geography

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The center of Newberry Volcano lies 20 miles (32 km) to the south of the city of Bend,[3] at the intersection of Deschutes, Klamath and Lake counties in Oregon,[4] where it is one of the most accessible volcanoes in the state.[5] It is the largest volcano in the Cascade Volcanic Arc at 620 square miles (1,600 km2),[6] and has roughly the same area as the state of Rhode Island[4] at 1,200 square miles (3,100 km2)[7] if its lava flows are included.[8] Newberry lies 37 miles (60 km) east[9] of the major crest of the Cascade Range in the High Lava Plains region,[7] rising 3,500 feet (1,100 m) above its surroundings.[3] From north to south, the volcano runs for a length of 75 miles (121 km), with a width of 27 miles (43 km)[7] and a total volume of about 140 cubic miles (600 km3).[9] Because of its enormous size and topographic prominence, it is often confused for an entire mountain range.[3]

Newberry Volcano has a somewhat dry climate due to its location in the rain shadow of the Cascade Range.[10] Climate data for the Newberry National Volcanic Monument are collected at the Lava Butte cinder cone, which had an average annual precipitation of 17.9 inches (455 mm) from 2002 to 2012.[11] Summer temperatures average from 73 to 82 °F (23 to 28 °C),[12] dipping to average minimum and maximum temperatures of −1.8 to 68.9 °F (−18.8 to 20.5 °C) during the winter season.[11] Spring has average temperatures of 60 °F (16 °C), while fall temperatures average 67 °F (19 °C).[12] Each year, total precipitation consisting of winter snow and summer rain varies from 9.8 to 29.5 inches (25 to 75 cm) in the highest parts of the region, and surface runoff rarely occurs even during heavy rain showers.[13] Only one stream appears on Newberry's entire surface, and it remains unclear whether the volcano has ever been able to support glaciers on its slopes,[10] since the mountain lacks cirques (amphitheater-like valleys formed by glacial erosion) or evidence of contact between lava and ice.[14] However, displaced glacial erratics have been found far from their native areas, moraine sediment has been deposited on the eastern and northeastern slopes of the volcano, and the mountain's various cone features have "boat" shapes that indicate glacial alteration.[15] The precise history of glaciers on the volcano is debated,[14] but dry channels and dry waterfalls on the eastern and western slopes are evidence that the volcano once held water.[16][17]

Aerial view of Paulina Lake and East Lake seen from the east

The volcano has two crater lakes, Paulina Lake and East Lake, which are filled by precipitation and percolation of ground water.[18] Paulina Lake occupies an area of 1,530 acres (6.2 km2) and reaches a maximum depth of 250 feet (76 m), and it is separated from East Lake by a narrow isthmus, which is composed of rhyolite lava.[19] East Lake has a smaller area of 1,050 acres (4.2 km2) with a maximum depth of 180 feet (55 m).[20] The lakes have historically flooded channels surrounding the volcano. A large flood between 4,000 and 2,300 years ago released up to 12,000 acre feet (0.0148 km3) in volume from Paulina Lake,[18] filling the valley floor above the Paulina Prairie,[21] downstream of the lake.[22] It was possibly caused by the failure of a rock ledge 5 feet (1.5 m) in height, rather than eruptive activity.[21] Another flood took place in 1909 on the Deschutes River downstream from where it meets its tributary the Little Deschutes River.[21]

Ecology

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The Newberry National Volcanic Monument forms part of the northern section of the Mazama Ecological Province,[11] which has soil comprised by aeolian pumice and volcanic products[23] over basalt bedrock.[24] Flora within the Newberry Volcano area includes forests of juniper,[25] whitebark pine,[26] ponderosa pine (including Oregon's largest ponderosa pine tree), lodgepole pine, jack pine, and white fir, in addition to other plants like Indian paintbrush, purple penstemon, bitterbrush, manzanita, and snowbrush.[27] Infestations by mountain pine beetles have killed many lodgepole pines in the area.[28] Animals near Newberry Volcano include burrowing owls, kangaroo rats, lizards, bats, rattlesnakes, eagles, porcupines, otters, bobcats,[12] mule deer, Roosevelt elk,[29] ducks,[30] and American pika.[31]

Lava flows from Newberry display varied vegetation cover, and there are variable levels of flora between flows, though the level of vegetation and species diversity generally increase with elevation. Dominant plant species on lava flows include oceanspray and wax currant, with rabbitbrush also common. Though forbs are not widespread on the lava flows, where they do occur Davidson's penstemon and hotrock penstemon dominate. Above elevations of 4,890 feet (1,490 m), roundleaf alumroot is common, particularly near the edges of lava flows. All lava flows support patches of grasses such as Idaho fescue, especially on north-facing slopes. One lava flow at Lava Butte is barren except for scattered, dense patches of greenleaf manzanita.[24]

The Lava Cast Forest is a group of trees molded by lava from an eruption 6,000 years ago.[28] Today, the surrounding site lies within the Newberry National Volcanic Monument and includes 11 kīpukas, plots of land surrounded by one or more younger lava flows. These habitat islands range from 0.74 to 279.23 acres (0.3 to 113 ha) in area and sustain forests that have not been significantly altered by humans other than nearby fire suppression and land management efforts. Consisting of pure and mixed forest stands, these forests include ponderosa pine, lodgepole pine, and grand fir/white fir hybrid trees, which are supported by young soils derived from Mazama pumice.[32]

Geology

[edit]
The diagram displays the movement of the North American tectonic plate with an arrow moving from right to left, with ovular shapes indicating the age progression of centers of rhyolitic (silicic) lavas. From right to left, three major volcanic centers are indicated with concentric circles, Yellowstone Caldera to McDermitt Caldera to Newberry Caldera
Progression of ages of rhyolitic (silicic) lavas and calderas from McDermitt Caldera to Newberry and Yellowstone calderas (red circles: MC, NC, & YC). Numbers are ages in millions of years.

KBML = Klamath–Blue Mountains Lineament
HLP = High Lava Plains
EDZ = Eugene–Denio Zone
BFZ = Brothers Fault Zone
SMF = Steens Mountain Fault
VF = Vale Fault
NNR = North Nevada Rift

White arrow shows direction of North American plate. Edge of the craton is approximately along the Oregon–Idaho border. Triangles are Cascades volcanoes.

Overlapping with the northwestern corner of the Basin and Range Province,[33] also known as the High Lava Plains, Newberry Volcano lies within a Cenozoic highland marked by normal faults known as the Brothers Fault Zone.[34] It is situated at the intersection of the Brothers Fault Zone with the north–northwest-trending Sisters and northeast-trending Walker Rim fault zones.[6] In the mantle under Newberry Volcano, P and S seismic waves exhibit an unusually low wave velocity.[9] The Earth's crust thins from 31 miles (50 km) at the nearby Three Sisters volcano complex to 22 miles (35 km) near Newberry, where it has a high Poisson's ratio.[9]

The oldest rocks in this region include silicic (rich in silica) lava domes from the late Miocene or early Pliocene, which lie near the province's eastern and southern borders, respectively.[34] Volcanism in this area suggests a progression of silicic eruptions, known as the Newberry Trend,[35] that moves in a northwest-trending direction[36] from the Harney Basin to Newberry Volcano and the rest of the Cascade Range.[37] Newberry Volcano's origins are somewhat controversial; some scientists think it originated from an independent hotspot,[38] but overwhelming evidence suggests that it is part of the Cascade Arc[39] and was produced by the subduction of the oceanic Juan de Fuca and Gorda tectonic plates under the continental North American Plate.[40] However, Newberry Volcano has been transformed by tectonic processes,[41] possibly related to subductive mechanisms[40][42] that enhance melting of the Juan de Fuca tectonic plate.[43] The High Lava Plains Trend,[44] or the Newberry Trend, moves at an oblique angle to the underlying North American tectonic plate,[36] for which subduction counterflow, gravitational flow along the lithosphere's base, faulting, and extension of the Basin and Range Province have all been proposed as possible mechanisms.[45] At Newberry, the subducting plate has a depth that is 12 to 31 miles (20 to 50 km)[9][42] shallower than elsewhere in the major crest of the Cascades,[b] accounting for its unique magmas.[42] Newberry Volcano is likely fed by a magma chamber 1.9 to 3.1 miles (3 to 5 km) under the large, cauldron-like caldera at its summit.[33][46] This caldera has dimensions of 4.0 by 5.0 miles (6.5 by 8 km) and formed about 75,000 years ago.[9]

Newberry Volcano first formed about 600,000 years ago[47][48] and has since been built up by several thousand eruptions.[47] About 500,000 years ago, Mount Newberry attained an elevation of 14,000 feet (4,300 m).[49] The caldera-forming event occurred about 75,000 years ago from a major explosive eruption.[50] It formed the crater lakes and Paulina Peak—which is the highest point on the volcano,[49] at 7,989 feet (2,435 m).[1][a]

As a result of its caldera-forming eruption,[33] Newberry has a horizontal profile, which is typical of a shield volcano.[3] However, it is also considered a composite volcano, made up of a matrix of lava flows and pyroclastic deposits.[3] Unlike more typical composite volcanoes in the Cascades, it formed from several eruption types including more traditional explosive eruptions and more fluid effusive events;[7] thus it is usually classified as a "shield-shaped composite volcano", or shield-shaped stratovolcano.[51] The volcano has a caldera at its summit, which has a diameter of 4 by 5 miles (6.4 by 8.0 km) and features two crater lakes: Paulina Lake and East Lake.[3] This caldera, known as the Newberry Crater, is forested, with small parts of its surface covered with lava flows and pumice deposits.[52] Before the caldera's creation, the mountain's summit was 500 to 1,000 feet (150 to 300 m) greater in height than its current elevation.[53] The caldera has reformed several times throughout the volcano's history, burying the caldera floor to a depth of 1,640 feet (500 m)[54] and creating concentric calderas, each smaller than its predecessor.[52] The first caldera—the volcano's largest caldera, forming approximately 300,000 years ago—was produced by the eruption of 2.5 cubic miles (10 km3) of pyroclastic ejecta, which created the Tepee Draw tuff and ash deposits that cover the volcano's eastern flank.[52] The last crater formed after an explosive eruption about 80,000 years ago, which ejected up to 2.5 cubic miles (10 km3) of pyroclastic materials.[55] Throughout this progression, the volcano shifted from rhyodacitic pumice to basaltic ash flows, the latter producing the Black Lapilli tuff that covers the western side of the volcano.[56] Since the last caldera-forming eruption 80,000 years ago, the volcano has undergone silicic eruptions at the caldera and produced basaltic and basaltic andesite lava flows that extended down its outer flanks.[56] The tephra and ash from the Black Lapilli tuff by the caldera formed agglutinates around its rim.[18] Newberry Volcano is cut by several fault scarps, small step offsets on the ground surface where one side of a fault has moved vertically with respect to the other.[57]

At the center of the isthmus that separates Newberry Volcano's two crater lakes is the central volcanic cone, named Central Pumice cone, which reaches 700 feet (210 m) above East Lake. With a broad, flat top,[20] it formed during an explosive eruption[58] about 7,000 years ago, and sits in the center of the caldera.[18]

Compositionally, lava from the Newberry Volcano has varied from primitive basalts with high magnesium levels to more evolved tholeiitic and calc-alkaline deposits[59] (based on the major element characteristics of the lavas).[60] Primitive lavas exhibit high abundances of chromium and nickel as well as variable concentrations of fluid-mobile elements like barium and strontium.[61] Tholeiitic and calc-alkaline lavas display overlap in magnesium, calcium oxide, and aluminum oxide levels but differ in that the tholeiites have lower contents of silica and potassium oxide and higher iron(II) oxide, titanium dioxide, and sodium oxide.[61] There is also much overlap in isotopic composition, though the tholeiitic lavas mark the low point for 87Sr/86Sr and the high point for 143Nd/144Nd and 176Hf/177Hf.[62] Examination of Newberry lavas with olivine-plagioclase hygrometry shows that tholeiites are anhydrous (less than 0.5 percentage by weight water) and thus distinct from calc-alkaline deposits (2–4 percentage by weight water); both have different fractional crystallization sequences that derive from primitive magmas, which had their compositions influenced by equilibrium with peridotite in the mantle.[60] By volume, basaltic andesite is the principal lava type at Newberry Volcano, with large volumes of silicic lava among older ash flow tuff deposits.[9]

Subfeatures

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The conical volcano Lava Butte and its central crater are seen from above, with the volcano's right half forested while the opposite side is largely barren. An access road flanks the cone.
Lava Butte, a cinder cone produced by eruptions at Newberry Volcano

Vents at the volcano follow north-east and north-west trends influenced by extension of the Basin and Range Province.[9] With more than 400 vents, Newberry has more individual subfeatures than any other volcano in the contiguous United States. These include cinder cones, lava domes, and various other lava edifices,[3] with at least 25 vents on the volcano's flanks and summits becoming active within the past 10,000 years.[47] Most of the cinder cones on the volcano's edifice vary from 200 to 400 feet (61 to 122 m) in elevation, though a number of them reach heights above 500 feet (150 m) with diameters greater than 1⁄2 mile (0.80 km). Most of these exhibit saucer-like summit depression landforms, with notable exceptions at Lava Top and North Kawak Buttes, which have craters that are 200 to 300 feet (61 to 91 m) in depth.[63] Basaltic and basaltic andesite lava flows have penetrated the bases of many of these cinder cones, forming a matrix of connected flows, and a veneer of pāhoehoe and ʻaʻā lavas can be found on Newberry volcano's northern and southern sides.[10] The northern flank holds three distinct lava tube systems that formed out of pāhoehoe lava: the Horse Lava Tube System (also known as the Horse System), Arnold Lava Tube System, and the Lava Top Butte basalt.[64]

About 7,000 years ago, at Newberry's Northwest Rift Zone,[65] lava fountains erupted from a fissure with a length of 1.5 miles (2.4 km),[66] yielding basaltic and andesitic lava flows.[67] Strombolian eruptions (which eject incandescent cinder, lapilli, and lava bombs) produced tephra that formed Lava Butte, a cinder cone near Newberry with a height of 500 feet (150 m),[66] a base diameter of 2,300 feet (700 m), and a crater depth of 160 feet (50 m). With a lopsided shape where the northeastern rim is 82 feet (25 m) taller than the southwestern counterpart,[68] this cinder cone sits 10 miles (16 km) south of Bend.[66]

The nearby Badlands shield volcano, which formed out of a rootless vent to produce a large basaltic lava flow at Newberry, has a diameter of 8 miles (13 km). It has pāhoehoe lava throughout its surface, with tumuli (mounds of earth and stones) and a pit crater.[10]

Dacite and rhyodacite domes can be found on the middle and upper flanks,[69] and Newberry also features twenty rhyolitic lava domes and lava flows among its western, eastern, and southern flanks.[10] These include East Butte and China Hat at the eastern base of the volcano, which date to 850,000 and 780,000 years ago, and therefore predate Newberry. The McKay Butte, found on the volcano's western side, formed 580,000 years ago. Other Holocene eruptions have produced rhyolite lava that remained close to the summit, including Paulina Peak, which has a width of one mile and reaches within 3 miles (4.8 km) of the wall of the caldera.[10]

Hot springs can be found at Paulina Lake and East Lake, along with one fumarole gas vent at Lost Lake, located near the Big Obsidian lava flow. These discharge gases like water vapor and carbon dioxide and give off a rotten smell, though the composition has few noxious components.[70]

Eruptive history

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A map shows the extent of lava flows emanating from Newberry Volcano under the extent of the volcanic center itself
Map showing lava flows from the Newberry Volcano

During the late Pleistocene, Newberry Volcano produced a number of voluminous lava flows, made of basalt, which originated from several vents on its northern flank and reached the modern areas of Bend and Redmond. They filled canyons that served as precursors for the Deschutes and Crooked rivers–since eroded–and extended tens of miles from the volcano. Lava from the last of these eruptions about 78,000 years ago covered the Bend area, surrounded the Pilot Butte cinder cone, and filled the Deschutes River bed.[71]

In addition to its production of large lava flows, Newberry Volcano has also produced a number of Plinian eruptions similar to the eruption of Vesuvius that destroyed Pompeii and Peléan eruptions like the 1902 explosion of Mount Pelée.[18] These include a number of caldera-forming eruptions, producing ash flow deposits including the Tepee Draw tuff and Black Lapilli tuff,[55] and rising 20 miles (32 km) or more into the stratosphere.[54] The last of these eruptions covered tens of thousands of square miles with ash, extending to the San Francisco Bay Area in California nearly 500 miles (800 km) to the southwest. Here, it reaches a thickness of one centimeter. Additionally, Newberry has produced multiple, voluminous explosive eruptions, with certain studies estimating up to 60 eruptive events of rhyolite and dacite tephra that reach Idaho, Utah, and northern California. These include the eruption that produced the Paulina Creek tephra between 55,000 and 50,000 years ago, and the eruption from 20,000 years ago responsible for the Wono tephra, which extends into western Nevada and east-central California. As a result of compositional zoning within the magma chamber that feeds the volcano, its ash deposits may show different chemical and mineralogical makeups.[56] The last of these tephra eruptions yielded the Newberry pumice just before 1,300 years ago, reaching several hundred miles to the east.[72]

Between the last Ice Age about 12,000 years ago and 7,700 years ago, the volcano erupted at least 12 times. Mount Mazama erupted 7,700 years ago, producing volcanic ash and pumice that accumulated to a thickness of up to 6 feet (1.8 m) on the Newberry Volcano, covering many of the lava flows on its slopes.[73] During three eruptive periods at Newberry over the past 7,500 years, the caldera has seen rhyolitic eruptions from seven individual vents.[74] About 7,000 years ago, eruptions occurred along the rift zone northwest of Newberry Volcano's caldera, yielding 12 lava flows that encompassed an area of 23 square miles (60 km2).[3] At about the same time, the Central Pumice cone was produced by eruptions that also formed the Interlake and Game Hut obsidian flows from a vent on the cone's southern flank. An eruption from a fissure zone at East Lake, 3,500 years ago, yielded tephra and formed the East Lake obsidian lava flows.[18]

The volcano underwent its most recent eruptions 1,300 years ago, producing the Big Obsidian flow. A silicic deposit, it is made up of rhyolite and features a number of lava blocks. Although it is frequently cited as the largest Holocene obsidian formation in the United States, its area of 1.09 square miles (2.8 km2) and volume of 0.031 cubic miles (0.13 km3) actually place it fifth in the nation.[75] The eruptions, which were both explosive and effusive, began with a Plinian explosion of pumice and tephra that covered the caldera's eastern half and reached several hundred miles to the east.[76] This deposit, called the Newberry pumice, reaches a thickness of 12 feet (3.7 m) up to 5.5 miles (8.9 km) from the vent that produced it, which is located at the southern flank of the caldera, and a thickness of 10 inches (25 cm) up to 40 miles (64 km) from the volcano.[77] Because of strong westerly winds, tephra reached as far east as Idaho.[78] This eruption also produced pyroclastic flows that left volcanic bombs in Paulina Lake.[77]

Recent activity and current threats

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Though Newberry Volcano is currently quiet,[79] the United States Geological Survey considers it an active volcano with a "very high" threat level.[4] Hot springs within the caldera remain active, and small earthquakes have occurred within recent local history.[79] Any future eruptions would likely show similar characteristics to eruptions from the past 15,000 years,[79] ranging from effusive production of lava flows to explosive eruptions ejecting pumice and ash.[80] If future lava flows from Newberry Volcano are of comparable size to its late Pleistocene eruptions, they would bury settlements throughout the Central Oregon region. They would also likely destroy segments of U.S. Route 97, disabling transportation in the area, in addition to likely ruining gas pipelines and power lines that extend electricity to California,[52] both of which would be accompanied by serious economic consequences.[81]

Flank lava flows, which would likely be basaltic in origin, might form lava fountains that could scatter cinders and lava for several thousand meters, building cinder cones or initiating forest fires. While the flows themselves move at rates of 30 feet (9.1 m) per minute, and thus could be escaped by animals and humans, they would destroy stationary structures in their paths. Pyroclastic flows, on the other hand, travel at speeds of 20 to 200 miles per hour (32 to 322 km/h), and their violent force could incinerate or pulverize objects in their path, or asphyxiate living things.[82]

Map of Oregon indicating Portland with a circle in the northwest, and major volcanoes indicated as triangles. Newberry is near the center of the state, under Three Sisters and above Crater Lake (Mount Mazama)
Newberry Volcano's location in Oregon relative to other major volcanoes

If another caldera-forming eruption of similar magnitude to previous ones at the volcano occurred, pyroclastic flows could devastate the area surrounding the volcano for up to 30 miles (48 km).[83] However, pyroclastic flows have been rare at Newberry.[84] Tephra from explosive eruptions would short-circuit electric transformers and power lines, clog engine filters, produce clouds that might yield lightning, and pose a hazard to aircraft overhead.[85] It would also pose health hazards because ash particles can irritate eyes, and when ingested, lungs, among other health issues.[86] Because of water from the two crater lakes, eruptions at Newberry Volcano may become more explosive and more likely to produce pyroclastic flows.[87] Moreover, if pyroclastic flows mix with snow or water overflowing from the crater lakes, they could spawn lahars, volcanically induced mudslides, landslides, and debris flows that could devastate the Paulina Creek valley and reach the La Pine valley within 30 minutes.[88] Threats from the volcano pose hazards to about 16,400 people who live within 19 miles (30 km) and more than 180,000 people living within 62 miles (100 km).[89]

In addition to threats from volcanic activity, at least one flood has taken place at Newberry Volcano in the past, though it may not have been a result of eruptive activity.[21] If lava flows from an eruption blocked the Deschutes River, they might generate floods upstream by increasing water level and downstream once the blockage clears.[90] Earthquakes unrelated to volcanic activity also take place in Oregon, though they are usually less than 2.5 on the Richter magnitude scale. Volcanoes can also cause earthquakes reaching magnitudes up to 5 on the Richter scale, which sometimes occur as swarms. These clusters of tremors cause shaking of houses, walls, and windows and can crack plaster or walls in older buildings but rarely cause major damage. Powerful earthquakes close to magnitude 7 would cause damage independently, but they would not cause Newberry Volcano to erupt unless it were already on the verge of activity.[91] Additional threats exist for rockfalls and avalanches.[74]

If Newberry Volcano were to erupt, it should be possible to detect increased seismic activity, while increased production of volcanic gas would likely kill trees near the volcano, which scientists would quickly recognize before notifying emergency management agencies.[92] Before 2011, Newberry was monitored by just one seismic station that had been installed in 1987 and had only detected seven earthquakes within 12 miles (19 km) of the volcano. In 2011, scientists from the Cascades Volcano Observatory installed eight more seismic and deformation monitors in the volcano's vicinity, which has seen the number of detectable earthquakes rise to 10–15 per year.[46] The volcano continues to be closely monitored by the United States Geological Survey, which monitors a seismometer network with the geophysics program at the University of Washington and regularly conducts leveling surveys to check for deformation that could suggest impending activity, in addition to sampling geothermal areas.[92] There are GPS instruments installed within the volcano's vicinity to monitor any swelling that occurs as a result of underground movement of magma.[93] Despite historical uplift at the volcano,[94] deformation has remained continuously low in recent years.[94][95]

Human history

[edit]
Black-and-white portrait of John Strong Newberry, the volcano's namesake
Newberry Volcano was named after John Strong Newberry (pictured), an American surgeon and geologist who explored central Oregon in the early 19th century, though he never actually visited the volcano itself

The area around Newberry Volcano has been inhabited by Native American peoples for more than 10,000 years, though only intermittently as a result of eruptive activity at the volcano and in the surrounding area. During an archaeological excavation near Paulina Lake in 1992, researchers discovered remnants of a central hearth and a housing structure with support posts and linear rock arrangements with dimensions of 13 by 16 feet (4.0 by 4.9 m). Radiocarbon dating of charcoal samples from the site were dated to 11,000 years ago. The mountain's caldera was used to harvest obsidian, which they used to sharpen arrowheads and tools and traded throughout the Pacific Coast region for several thousand years.[54]

The first recorded European to visit the volcano was Peter Skene Ogden, a trapper who reached the crater in 1826. In 1855, the volcano's namesake, John Strong Newberry, a surgeon and geologist for the Williamson and Abbot survey party, visited central Oregon while mapping the local area for the Pacific Railroad,[96] but never visited the volcano.[33] Paulina Lake, Paulina Creek, and Paulina Peak are named after Paulina, a Snake Indian chief who headed raiding parties against whites during the 1850s and 1860s before he was pursued and shot by settler Howard Maupin.[96] Near the end of the 19th century, the Lava River Cave was used by the hunter Leander Dillman to store perishable foods.[49] The name Mount Newberry was proposed by Israel Russell, who visited the area in 1903, though the name did not come into use. Instead, it was known as Newberry Crater until it was renamed to the Newberry Volcano in the 1930s by geologist Howel Williams, a name which was formally accepted in 2003 when geologist Larry Chitwood supported it through the official geographic naming process.[33]

Because of the efforts of Hollis Dole, head of the Oregon Department of Geology, to promote the area, in 1963 NASA scientists became interested in using lava fields at Newberry to prepare for the United States' first Moon landing.[97] NASA used the area in October 1964 and July 1966 to geologically train the Apollo Astronauts in recognizing volcanic features, such as cinder and pumice cones, lava flows, ash and obsidian flows, and a lava tube. Astronauts who would use this training on the Moon included Apollo 11's Neil Armstrong and Buzz Aldrin, Apollo 12's Alan Bean, Apollo 14's Edgar Mitchell, Apollo 15's James Irwin, and Apollo 16's Charlie Duke. Notable geologist instructors included Aaron Waters.[98]

The Newberry National Volcanic Monument was established in November 1990[99] by the United States Congress.[3] With an area of more than 54,000 acres (220 km2),[99] it forms a near-circular shape around the summit caldera and then a long corridor from the mountain's northwestern side to the Deschutes River that includes a rift zone.[3] The Monument lies within the Deschutes National Forest, which is managed by the United States Forest Service.[99] As of 1997, the caldera area of Newberry holds seven campgrounds, two resort areas, and six summer houses.[47]

Mining and geothermal energy

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Because Newberry has had recent eruptive activity, has remained active for a long time, and has a shallow heat source feeding hot springs, it represents a source of geothermal energy. An investigation conducted by the United States Geological Survey in 1981 drilled a well 3,057 feet (932 m) in depth at a location to the east of the Big Obsidian flow, finding temperatures of 509 °F (265 °C) under the surface there. An energy company drilled two holes with a depth of 10,000 feet (3,000 m) in 1995 and 1996, but they were unable to find fluids, so they lacked a mechanism to drive turbines and opted to end the project at Newberry. According to many scientists, Newberry Volcano represents the best geothermal energy candidate in the Pacific Northwest;[54] in 2012, a deep well was built to determine whether water directed into the hole might be heated and returned to the surface in order to yield energy.[100]

Recreation

[edit]
A hiker stands under the arched ceilings of the Lava River Cave, which was formed from a lava flow at Newberry Volcano
A hiker under the arched ceilings of a representative portion of Lava River Cave

Newberry Volcano is visited by 250,000 people each year, who come to go fishing for trout in East Lake, to camp on Paulina Lake, or go mountain biking around the 22 miles (35 km) loop that surrounds the crater.[49] The lakes are also popular for boating.[53] At the Newberry National Volcanic Monument, camping, fishing, and hiking are popular, including on the Trail of the Molten Land, which follows a 7,000-year-old lava flow from Lava Butte,[101] and the Trail of the Whispering Pines, which traverses a ponderosa pine forest.[12] Horse riding is also possible in a section of the Peter Skene Ogden Trail, 3 miles (4.8 km) long, which runs through the monument area; snowmobiling and cross-country skiing are also popular.[102]

The Lava Lands Visitor Center within the Monument has an exhibit on the area's geology and culture and offers a paved path that runs for 5.5 miles (8.9 km). A shuttle leaves from the center every 20 minutes during the peak season from Memorial Day through Labor Day, costing $2 per traveler. The area can also be accessed by personal motorized vehicles during off season with a permit from the visitor center, and the center's parking area remains open year-round.[103] The area offers eight campgrounds operated by the United States Forest Service.[104]

The last lava flow from Newberry during the Pleistocene formed the Lava River Cave, 12 miles (19 km) to the south of Bend. This feature is the state's longest continuous lava tube, which can be hiked for more than one mile to the north and west and has an arching ceiling with a thickness of 45 feet (14 m).[71] This trail represents the monument's most popular attraction and can be hiked between May and mid-September with a recreation day pass that costs $5.[49] Jackets are recommended, as the temperature within the cave is usually 40 °F (4 °C).[28] The Lava Cast Forest, a group of trees molded by lava from an eruption 6,000 years ago, covers an area of 5 square miles (13 km2) and can be observed from a paved, narrow, and steep one-mile trail.[28] The area was designated as the Lava Cast Forest Geological Area in April 1942 by the United States Forest Service, which included 5,120 acres (20.7 km2) of land in the region. Known to the American public since 1928, by the mid-1940s the Lava Cast Forest was visited by thousands of tourists each year.[97] In the mid-1970s, the region had 150,000 tourist visitors annually, with the Lava Lands Visitors Center built by the Forest Service in September 1975.[97]

The trail to the volcano's summit at Paulina Peak lasts 15.5 miles (24.9 km) from Highway 97, with an easy paved road to the caldera and four rest stops, though it grows steep and twisty near the end.[105] The winding trail near the end is made of gravel and lasts for three miles, offering views of Mount Hood, Mount McLoughlin, and the Three Sisters volcanoes.[106]

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Newberry Volcano

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Newberry Volcano is a broad, shield-shaped composite volcano located in , , spanning Deschutes, Klamath, and Lake counties at coordinates 43.722° N, 121.229° W, and covering an area of about 3,100 square kilometers (1,200 square miles), roughly the size of . Rising to an of 2,434 meters (7,986 feet), it has been active for approximately 500,000 years, producing a full range of lava types from to rhyolite through diverse eruptive styles, including effusive lava flows and explosive events. Its most recent eruption occurred around 1,300 years ago, forming the prominent Big Obsidian Flow, and it remains an with ongoing geothermal activity such as hot springs and fumaroles. The volcano's geological evolution began about 500,000 years ago with primarily basaltic eruptions that built a broad structure, followed by more silicic (rhyolitic) activity around 75,000 years ago that led to the collapse of its summit and the formation of an approximately 8-kilometer-long by 6.5-kilometer-wide containing and East Lakes. Over its history, Newberry has experienced thousands of eruptions, including ash flows, pyroclastic flows, and falls, with post-caldera activity producing notable features like flows and deposits within the , established in 1990 to protect its youngest volcanic landscapes. From the city of Bend to the north, the volcano appears as a gradual ridge rising about 1,220 meters (4,000 feet), underscoring its morphology despite the explosive elements in its record. As one of the largest volcanoes in the , Newberry poses significant hazards due to its proximity to population centers and infrastructure in , earning a "very high threat" designation in volcanic risk assessments. Potential future eruptions could generate lava flows advancing several kilometers, pyroclastic flows and surges confined mostly to the but capable of broader impacts, widespread fallout affecting air quality and agriculture, and emissions of volcanic gases like . Monitoring by the U.S. Geological Survey includes seismic networks detecting 10–15 earthquakes annually since 2011 and geodetic instruments tracking ground deformation, with no signs of imminent unrest as of 2025. The volcano's diverse eruptive potential and location near recreational areas highlight the importance of ongoing hazard mitigation and public awareness efforts.

Location and Geography

Physical Characteristics

Newberry Volcano is a large shield-shaped situated in , within Deschutes National Forest, approximately 20 miles (32 km) south of Bend in Deschutes, Klamath, and Lake Counties. It lies east of the crest amid high desert plateaus, with the glaciated summits of the Three Sisters volcanic cluster rising about 25 miles (40 km) to the west on the horizon. The volcano's broad, gently sloping form spans roughly 1,200 square miles (3,100 km²), measuring about 75 miles (120 km) north-south and 27 miles (43 km) east-west, with an estimated total volume of 120 cubic miles (500 km³). This makes it one of the largest volcanoes in the , comparable in areal extent to the state of . Rising from a topographic base at approximately 4,400 feet (1,340 m), the volcano's summit elevation reaches 7,984 feet (2,435 m) at Paulina Peak, providing panoramic views of the surrounding landscape. At its center, a large holds two deep lakes that occupy much of the basin floor.

Caldera Formation and Features

The Newberry Caldera, a prominent feature at the of Newberry , formed approximately 75,000 years ago following a series of massive explosive eruptions that emptied a shallow , leading to the of the overlying volcanic edifice. This event created a broad, oval-shaped depression measuring about 4 miles (6.5 km) wide by 5 miles (8 km) long, encompassing roughly 17 square miles (44 km²) and situated at elevations between 6,300 and 7,500 feet (1,920 and 2,290 m). The caldera's formation is part of a broader history of silicic at Newberry, with at least five such events documented over the volcano's lifespan, though the most recent defines the current topographic basin. Within the caldera, two large rift lakes dominate the landscape: Paulina Lake and East Lake, separated by a narrow central platform composed of rhyolitic lava flows and deposits. Paulina Lake, the larger of the two, covers 1,531 acres (620 ha) with a maximum depth of 250 feet (76 m), while East Lake spans 1,044 acres (422 ha) and reaches depths up to 180 feet (55 m). These lakes occupy much of the caldera's floor, fed primarily by precipitation, snowmelt, and subsurface hydrothermal inflows rather than surface streams, and they drain southward via Paulina Creek, which has incised a steep gorge through the western rim. Over 400 volcanic vents are scattered across the volcano, with many manifesting as cinder cones, spatter cones, fissure vents, and associated lava flows on the floor, many of which have been active in the . Notable examples include the Central Pumice Cone rising 700 feet (210 m) above East Lake and the Big Flow, a young rhyolitic dome and flow complex south of the lakes. Hydrothermal features are also prevalent, particularly around East Lake, where hot springs and fumaroles indicate ongoing heat from the underlying system, with surface manifestations including warm-water inflows and gas emissions.

Geology

Volcanic Composition and Structure

Newberry Volcano is a shield-shaped composite volcano characterized by a broad, gently sloping profile built primarily through the accumulation of to lavas. Its volcanic composition spans a wide range from to rhyolite, including intermediate varieties such as , , , and rhyodacite, reflecting diverse magmatic processes at the intersection of the Cascade Arc and the High Lava Plains. The edifice comprises layered deposits of effusive lava flows and pyroclastic materials, with early shield-building phases dominated by tholeiitic and calc-alkaline that form the foundational flanks, overlain by more evolved andesitic to dacitic domes and flows within the summit region. This compositional diversity arises from magma hybridization and differentiation, where inputs mix with silicic melts, producing bimodal basalt-silicic assemblages that exhibit both effusive and explosive eruptive styles. The volcano's formation began approximately 600,000 years ago, with an estimated total volume of 400–500 km³ of erupted material, potentially up to 800–1,000 km³ when accounting for subsurface intrusions and erosion. Structural evolution involved progressive layering of basaltic shield lavas, which constructed the main edifice over hundreds of thousands of years, followed by the development of more viscous intermediate to felsic domes that added stratovolcano-like features to the otherwise shield-dominated morphology. Geological mapping classifies the volcanic facies by lithology and composition, delineating zones of mafic flank flows transitioning to silicic central deposits, as detailed in USGS Scientific Investigations Map 2455. Internally, Newberry's structure includes a complex magma system inferred from , featuring a at depths of 3–6 km beneath the , interpreted as a partially molten with estimated volumes of up to ~60 km³ from (poorly resolved) or 2–8 km³ from waveform modeling. This chamber exhibits evidence of fractional crystallization, where cooling and differentiation of basaltic parent magmas generate the observed range from to rhyolitic compositions through crystal settling and melt evolution. Drilling data from the USGS N-2 well further reveal stratigraphic layering within the fill, confirming the transition from older basaltic substrates to younger silicic units.

Major Subfeatures

Newberry Volcano exhibits a diverse array of volcanic landforms, including cinder cones, obsidian flows, and erosional features shaped by post-eruptive processes. Among the prominent peripheral cinder cones is , a 500-foot-high (152 m) structure formed approximately 7,000 years ago through basaltic eruptions along the volcano's northwest . This cone, along with others like Tumalo Cone on the north flank, exemplifies the volcano's monogenetic vents that produced localized pyroclastic deposits and associated lava flows, contributing to the shield's broad topographic profile. The flows represent another key subfeature, characterized by their glassy texture resulting from rapid cooling of high-silica rhyolitic . The Big Obsidian Flow, the most notable example, erupted about 1,300 years ago within the and covers over 2.6 square kilometers (1 ), consisting primarily of and that preserve the flow's internal structures. These flows highlight the volcano's capacity for viscous, silicic eruptions distinct from its dominant basaltic activity. Erosional landforms further define the volcano's periphery, including Paulina Creek Falls, where water exiting the incises through ancient deposits, creating a twin 80-foot (24 m) drop over pyroclastic cliffs. Similarly, basalt flows from Newberry have interacted with the , filling and damming its paleo-channel to form steep-walled canyons that expose layered volcanic sequences up to 150 feet (46 m) deep. These features underscore the interplay between eruptive deposition and fluvial in shaping the landscape. Overall, Newberry's subfeatures reflect its morphology, with gentle slopes built by fluid lavas from fissure vents, interspersed with localized pyroclastic cones and more explosive rhyolitic products. This diversity arises from a compositional range spanning to rhyolite, as detailed in the volcano's .

Eruptive History

Prehistoric Eruptions

The prehistoric eruptive history of Newberry Volcano commenced with an initial shield-building phase approximately 600,000 to 100,000 years ago, dominated by voluminous eruptions of lava flows that constructed a broad, low-relief spanning more than 1,200 square miles (3,000 km²). These effusive events, sourced from numerous flank and summit vents, accumulated to form the foundational structure of the volcano, with total erupted volumes exceeding 500 km³ over its lifetime, much of it from this early activity. A pivotal shift to silicic occurred around 400,000 to 300,000 years ago, marked by catastrophic caldera-forming eruptions that ejected large volumes of rhyolitic ash-flow tuffs, estimated at several tens of cubic kilometers per event. These highly eruptions, involving compositionally evolved magmas, led to the collapse of early nested calderas within the developing edifice, reshaping the summit and depositing widespread layers across . The most recent major caldera-forming event, dated to about 80,000 years ago, produced a compositionally zoned rhyolitic to andesitic ash-flow that triggered the forming the present 6.5 by 8 km . In the ensuing period from roughly 70,000 to 10,000 years ago, post- resurgence involved dome-building eruptions of rhyolite, such as the Paulina Peak dome (dated to 83 ± 5 ka), alongside andesitic lava flows that partially infilled the basin and contributed to intracaldera features like the north caldera wall. Dating of these prehistoric events relies on tephra correlations, such as with the Flat tephra, and paleomagnetic analyses of volcanic units, including the of Lava Top (~75–80 ka), supplemented by ⁴⁰Ar/³⁹Ar methods on key lavas like the ~400 ka of Crooked River Gorge. These techniques reveal a complex sequence of mafic-to-felsic transitions that established the volcano's bimodal composition and structural framework.

Holocene and Recent Activity

The epoch, beginning approximately 11,700 years ago, has been marked by at least 25 eruptions at Newberry Volcano, primarily consisting of basaltic fissure eruptions on the flanks and rhyolitic explosive events within the . These activities followed the retreat of the last , with early Holocene eruptions including a major explosive event around 9,500 years ago that produced significant rhyolitic tuffs and ash deposits. Later in the epoch, around 7,700 years ago, a series of rhyolitic lava flows and domes formed within the , contributing to features like the Interlake Obsidian Flow. Basaltic eruptions on the volcano's northwest were also prominent during this period, exemplified by the event at approximately 7,000 years ago, which generated a , extensive fluid lava flows extending up to 20 miles (32 km), and blankets. The most recent major eruption occurred around 690 AD (approximately 1,300 years ago) at the Big Obsidian Flow on the south wall, beginning with an explosive phase that ejected rhyodacitic ash and reaching as far as , followed by the extrusion of an obsidian dome and thick lava flow; this event had a (VEI) of 4. An additional rhyolitic eruption may have occurred around 490 AD on the south wall, also rated VEI 4, producing ash and . The U.S. Geological Survey (USGS) Cascades Volcano Observatory currently monitors Newberry Volcano for signs of unrest through a network of seismometers, GPS stations for ground deformation, and occasional gas sampling. Seismicity has remained low since a 2011 swarm associated with enhanced geothermal system testing, with an average of 10-15 small earthquakes per year within the caldera and no patterns indicative of magma movement. Ground deformation is minimal, and fumarolic gas emissions from hot springs show no anomalous increases; as of November 2025, there are no signs of an imminent eruption, though recent seismic upticks in 2024 were attributed to non-volcanic geothermal exploration activities. Potential hazards from future eruptions at Newberry would likely mirror events, including fluid basaltic lava flows capable of traveling 10-20 miles (16-32 km) from flank vents and threatening nearby communities like Bend and Sunriver. Rhyolitic eruptions in the could generate pyroclastic flows—hot avalanches of gas, ash, and rock fragments—that rapidly descend slopes, as evidenced by preserved deposits from past events, and lahars (volcanic mudflows) triggered by or rainfall on fresh ash. eruptions have reached VEI 4, with plumes up to 20 km high, but larger events up to VEI 5 remain possible based on the 's history of explosive activity.

Ecology

Flora and Fauna

The diverse flora of Newberry Volcano reflects its varied elevation gradients, ranging from approximately 4,000 to 8,000 feet, creating hotspots with a wide array of plant communities adapted to volcanic soils, lava flows, and hydrothermal influences. Dominant vegetation includes ponderosa pine forests on lower slopes, transitioning to lodgepole pine and mixed conifer stands at mid-s, with white fir, western juniper, aspen, grand fir, and Douglas-fir contributing to multi-layered canopies in late successional areas. Subalpine meadows occur at higher elevations, supporting wildflowers such as Davidson's , Pacific lupine, and hoary aster, while riparian zones around lakes feature willows, sedges, and other moisture-dependent species that stabilize shorelines and provide connectivity. An endemic , the grape-fern (Botrychium pumicola), thrives in deposits unique to the volcano's eruptive history, highlighting localized adaptations to harsh substrates. Fauna at Newberry Volcano is equally varied, with mammals such as , black bears, and coyotes inhabiting forested slopes and open areas, while smaller species like golden-mantled ground squirrels, yellow-pine chipmunks, pikas, and long-tailed weasels occupy lava flows and meadows. Cougars, as apex predators, range across the , preying primarily on deer in these habitats. Birdlife is abundant and diverse, including bald eagles and ospreys nesting near lakes, as well as Clark's nutcrackers, , , yellow-rumped warblers, , downy woodpeckers, and foraging in forests. Reptiles such as western fence lizards, western skinks, and garter snakes, along with amphibians like western toads and Pacific tree frogs, are found in wetter microhabitats, while bats including and long-eared myotis roost in caves and feed on insects over lava fields. Aquatic ecosystems in the caldera lakes support robust fish populations, with Paulina Lake and East Lake stocked with and , alongside native or established that feed on in the nutrient-rich waters. These lakes, formed within the , also host , contributing to a productive influenced by geothermal inputs. Hydrothermal vents and hot springs in the vicinity sustain unique microbial mats, particularly thick bacterial communities in deeper lake zones below the photic layer, which form the base of specialized aquatic food webs.

Environmental Dynamics and Threats

Following volcanic eruptions at Newberry Volcano, begins with such as lichens and mosses colonizing barren lava flows and ash deposits, gradually building soil through weathering and over centuries to millennia. These early colonizers pave the way for herbaceous plants and shrubs, eventually transitioning to coniferous s dominated by species like ponderosa pine and lodgepole pine, as observed on lava flows such as the Big Obsidian Flow from approximately 1,300 years ago. This primary succession process, driven by substrate stabilization and organic matter accumulation, can take thousands of years to reach mature stages in the arid environment. Climate change is altering environmental dynamics around Newberry Volcano through warming temperatures, projected to increase by up to 4.7°C by the late , and reduced leading to earlier and diminished summer streamflows. These shifts have caused fluctuations in lake levels, with East Lake and Paulina Lake experiencing lower summer volumes—potentially declining by 40-60% in stream inflows by 2040—exacerbating for aquatic habitats and promoting warmer lake surface temperatures that stress cold-water species. Species migration is evident, with cold-adapted fish like facing habitat contraction and potential local extirpation due to thermal barriers, while warmer conditions facilitate upward elevational shifts in montane and bird distributions. Additionally, prolonged growing seasons may accelerate the spread of , such as cheatgrass () and western juniper (), which outcompete native bunchgrasses and sagebrush in disturbed areas, further altering ecosystem composition. Non-volcanic threats compound these pressures, including intensified that fragment habitats and release nutrients promoting post-fire invasives. The 2017 wildfire season in burned over 665,000 acres in the region, including parts of Deschutes National Forest, demonstrating how severe fires can lead to , reduced water retention, and shifts toward non-native vegetation dominance in recovery phases. contributes to water quality degradation in the caldera lakes through increased loading from human activities near hot springs, fostering occasional cyanobacterial (blue-green ) blooms that impair swimmer safety and aquatic oxygen levels, particularly in shallow, geothermal-influenced zones. from recreational trails and road networks also disrupts wildlife corridors, isolating populations of mammals and birds in the diverse volcanic terrain. Geothermal activity influences aquatic life in the caldera lakes, where volcanic CO₂ inputs to East Lake—totaling around 11,700 tons annually—enhance primary productivity by supplying carbon for photosynthesis, resulting in organic-rich sediments (6-12% carbon content) that support a unique geogenic food web. However, elevated CO₂ degassing in hotspots (up to >90% of lake flux) and trace mercury (up to 13 ppm) pose potential risks to fish and invertebrates, though current levels show minimal bioaccumulation; conservation studies emphasize ongoing monitoring to mitigate gas hazards without disrupting this high-productivity ecosystem. Recent assessments from the 2020s highlight biodiversity loss driven by these dynamics, with projections of shrubland decline (e.g., big sagebrush) replaced by drought-tolerant invasives, underscoring the need for adaptive management in south-central Oregon's volcanic landscapes. As of 2024-2025, ongoing geothermal exploration projects, including enhanced geothermal systems (EGS) drilling, have increased seismic activity (10-15 earthquakes annually), potentially impacting local habitats and requiring environmental monitoring to assess effects on ecology.

Human History

Indigenous and Early Settlement

The Newberry Volcano region has been a significant for Indigenous peoples, particularly the Northern Paiute, Klamath, and , for over 10,000 years. These groups established seasonal camps and utilized the area's resources, including fishing in Paulina and East Lakes, which provided abundant and , and hunting in surrounding forests and meadows. The harsh volcanic terrain, characterized by lava flows and limited arable land, precluded permanent villages, but the served as a hub for seasonal gatherings and resource procurement. Central to Indigenous use was the quarrying of obsidian from flows like the Big Obsidian Flow, a material prized for crafting tools such as arrowheads, spears, and knives, as well as ceremonial items. This obsidian was traded along extensive networks, including trails paralleling modern Highway 97, connecting to Columbia River sites like Celilo Falls. Archaeological evidence, including the Paulina Lake Site excavated in 1992, reveals hearths, stone tools, and the remains of a 9,500-year-old wickiup-style structure made from lodgepole pine, underscoring continuous occupation dating back at least 10,000 years. Tribal oral histories describe the volcano as a sacred place and a gift from the Creator, with some flows emerging during eruptions witnessed by ancestors, embedding the landscape in spiritual narratives. European-American interactions began in the early 19th century with fur trappers like Peter Skene Ogden, who explored the caldera vicinity in 1826 while mapping routes through central Oregon. In 1843, John C. Frémont's expedition traversed nearby trails during his southward survey from Oregon to California, documenting the region's geology and indigenous pathways without directly entering the caldera. By the mid-19th century, U.S. military presence increased amid conflicts, with Northern Paiute people, led by Chief Paulina, using the rugged terrain as a hideout during the 1860s Paiute War. Settlement expanded in the late 1860s as ranchers from the Willamette Valley drove cattle eastward for grazing on the bunchgrass prairies surrounding the volcano, followed by initial timber harvesting in the 1870s to support regional growth. These activities marked the transition to non-Indigenous land use, displacing traditional practices as tribes were forcibly relocated to reservations like Warm Springs and Klamath by the late 19th century.

Exploration, Mining, and Resource Use

Scientific exploration of Newberry Volcano intensified in the early 20th century through efforts by the U.S. Geological Survey (USGS). In 1903, geologist Israel C. Russell conducted a survey of as part of a broader assessment of the region's geology and , focusing on the volcano's andesitic structure, eroded summit amphitheater, post-glacial s, and associated lava flows. His observations, detailed in a 1905 preliminary report, provided the first systematic description of the volcano's topographic and geological features, including measurements of crater dimensions and cliff heights, though limited by the absence of precise surveying instruments. This work laid foundational mapping for subsequent studies, emphasizing the volcano's potential as a water source amid its volcanic landforms. Mining activities at Newberry Volcano were modest and centered on volcanic materials like and . from flows within the , valued historically by for tool-making, saw limited extraction in the early to mid-20th century for abrasives and grinding applications, though commercial operations remained small-scale due to accessibility challenges and shifting industrial demands. mining began sporadically post-World War II, with claims staked on the Central Pumice Cone before 1945 yielding block for abrasives over nearly 50 years; production was constrained to small volumes, leaving substantial reserves untapped amid environmental considerations. Geothermal prospecting emerged as a key focus in the , driven by the volcano's high heat flow and hydrothermal potential. In , the USGS drilled the Newberry 2 well to a depth of 932 meters in the central , encountering temperatures up to 265°C (509°F) in fractured basalts, indicating viable subsurface reservoirs but revealing hydrothermal alteration minerals like and . Efforts by the USGS and private entities, such as the 1981 test hole, confirmed elevated geothermal gradients but were halted due to risks and economic hurdles, though the data underscored the site's promise for . Post-2010 research advanced enhanced geothermal systems (EGS) at Newberry, building on earlier findings to test techniques for heat extraction. The 2010–2014 EGS Demonstration project, led by AltaRock Energy with U.S. Department of Energy funding, involved hydraulic of existing wells like NWG 55-29, achieving flow rates and temperatures suitable for power generation while monitoring seismic activity to mitigate hazards. Environmental assessments for these operations evaluated impacts on , , and , concluding minimal surface disruption with no significant adverse effects from low-volume fluid injections. Recent developments, including Mazama Energy's test reaching 332°C (629°F) in an engineered reservoir—announced as the world's hottest EGS with potential to power 25,000 homes using 75% less than conventional systems—highlight ongoing potential for scalable clean to support centers, with further assessments emphasizing sustainable fluid circulation to avoid interference.

Recreation and Protection

Visitor Activities

Newberry National Volcanic Monument offers a variety of opportunities, including the challenging Paulina Peak Trail, a 6.1-mile out-and-back route that ascends 1,617 feet to the 7,985-foot summit for panoramic views of the , Cascade Mountains, and high desert. Another popular option is the approximately 21-mile Crater Rim Trail, which circumnavigates the Newberry and provides access to diverse volcanic landscapes, though backpackers should prepare for rugged terrain and obtain necessary permits from the U.S. Service. Shorter interpretive paths, such as the 0.8-mile loop through the Big Obsidian Flow, allow visitors to explore jagged fields formed by a 1,300-year-old eruption, with boardwalks facilitating safe navigation over the sharp . Water-based recreation centers on Paulina Lake and East Lake within the , where non-motorized boating, , and are permitted from designated launches. Anglers target , , and in these lakes, with shore and boat fishing opportunities enhanced by seasonal stockings from the Department of Fish and Wildlife; catch-and-release practices are encouraged to sustain populations. is available at developed sites like Paulina Lake Campground, offering 69 sites with amenities such as picnic tables, fire rings, and vault toilets, reservable through Recreation.gov from May to . Lava tube exploration highlights include the , a 1-mile-long intact formed about 100,000 years ago, accessible via a self-guided walk that requires sturdy shoes, warm clothing, and a due to the constant 42°F temperature and uneven surfaces. Peak summer access via paved roads to the , while winter conditions limit entry to snowshoeing and from trailheads like 10 Mile Sno-Park, leading to sites such as Paulina Falls. Backcountry users must secure free permits for overnight stays in designated areas to minimize impact on sensitive ecosystems. Educational programs at the Lava Lands Visitor Center focus on the monument's and , featuring ranger-led tours of Lava Butte's summit via aerial tram, interactive exhibits on volcanic processes, and guided cave explorations that explain lava tube formation and preservation. These sessions, offered seasonally from to , cater to families and school groups, emphasizing the interplay of volcanic activity and local without requiring advance reservations for most public programs.

Conservation Efforts and Management

In 1990, the was established under 101-522 to preserve the volcano's unique geologic landforms, ecosystems, and cultural resources, encompassing approximately 54,000 acres within the Deschutes National Forest. Managed by the U.S. Forest Service, the monument's designation withdrew the area from new mining claims and other forms of public land disposal to prevent resource extraction that could damage lava flows, fields, and lakes. The comprehensive management plan, finalized in 1994, outlines standards for five zones, including protections for wilderness areas and riparian habitats, while allowing sustainable recreation under the Northwest Forest Plan. The U.S. Geological Survey (USGS) integrates volcanic monitoring with monument conservation through the Cascades Volcano Observatory, assessing hazards to inform land-use decisions and protection. Seismic networks, upgraded in 2011, detect earthquakes averaging 10–15 per year within the , aiding in the evaluation of unrest that could affect habitats. Deformation monitoring via GPS and leveling surveys tracks subtle ground changes, supporting Forest Service efforts to mitigate risks to sensitive lake and . These activities align with conservation by providing data for emergency planning and habitat restoration, as outlined in USGS hazard summaries. Restoration initiatives in the monument focus on post-disturbance recovery, including invasive species prevention in aquatic environments like East Lake and Lake, where Oregon state permits are required for watercraft to curb introductions of non-native organisms. In the broader Deschutes National Forest, collaborative projects under the 2013 Forest Landscape Restoration initiative address resilience through prescribed burns—targeting up to 9,000 acres in spring 2025, which treated 2,580 acres—and mechanical thinning to restore native vegetation and reduce fuel loads near the monument. Challenges include balancing increasing , which fragments habitats through trail erosion and disturbance, with protection measures, as highlighted in ecoregional assessments. Climate adaptation strategies, informed by vulnerability studies for south-central , emphasize maintaining lake hydrology and riparian buffers to counter warming effects on aquatic ecosystems, such as altered water levels and species shifts.

References

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  10. https://www.recreation.gov/camping/campgrounds/233196
  11. https://www.recreation.gov/camping/campgrounds/251447
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  33. https://www.oregon.gov/oda/Documents/Publications/PlantConservation/BotrychiumPumicolaProfile.pdf
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  41. https://sos.oregon.gov/blue-book/Pages/explore/monuments/newberry-deur.aspx
  42. https://www.oregonencyclopedia.org/articles/newberry_national_volcanic_monument/
  43. https://www.oregonhistoryproject.org/narratives/central-oregon-adaptation-and-compromise-in-an-arid-landscape/pre-industrial-period-1870-1910/settlement/
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  56. https://natureconnectco.org/lava-lands-tours/
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  63. https://deschutescollaborativeforest.org/
  64. https://www.centraloregondaily.com/news/local/deschutes-national-forest-spring-prescribed-burns/article_9306e503-ddb2-44ce-8476-3d265cc1d837.html
  65. https://deschutescollaborativeforest.org/2025-spring-prescribed-fire-season-wraps-up/
  66. https://www.oregonconservationstrategy.org/ecoregion/east-cascades/
  67. https://wpg.forestry.oregonstate.edu/sites/default/files/bibliopdfs/pnw_gtr974.pdf
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