Mauna Loa (/ËŒmÉ"ËnÉ™ ˈloÊŠ.É™/ or /ËŒmaÊŠnÉ™ ˈloÊŠ.É™/; Hawaiian: [ˈmÉ"unÉ™ ˈlowÉ™]; English: Long Mountain) is one of five volcanoes that form the Island of Hawaii in the U.S. state of HawaiÊ»i in the Pacific Ocean. The largest subaerial volcano in both mass and volume, Mauna Loa has historically been considered the largest volcano on Earth. It is an active shield volcano with relatively shallow slopes, with a volume estimated at approximately 18,000 cubic miles (75,000 km3), although its peak is about 120 feet (37 m) lower than that of its neighbor, Mauna Kea. Lava eruptions from Mauna Loa are silica-poor and very fluid, and they tend to be non-explosive.
Mauna Loa has probably been erupting for at least 700,000Â years, and may have emerged above sea level about 400,000Â years ago. The oldest-known dated rocks are not older than 200,000Â years. The volcano's magma comes from the Hawaii hotspot, which has been responsible for the creation of the Hawaiian island chain over tens of millions of years. The slow drift of the Pacific Plate will eventually carry Mauna Loa away from the hotspot within 500,000 to one million years from now, at which point it will become extinct.
Mauna Loa's most recent eruption occurred from March 24 to April 15, 1984. No recent eruptions of the volcano have caused fatalities, but eruptions in 1926 and 1950 destroyed villages, and the city of Hilo is partly built on lava flows from the late 19th century. Because of the potential hazards it poses to population centers, Mauna Loa is part of the Decade Volcanoes program, which encourages studies of the world's most dangerous volcanoes. Mauna Loa has been monitored intensively by the Hawaiian Volcano Observatory since 1912. Observations of the atmosphere are undertaken at the Mauna Loa Observatory, and of the Sun at the Mauna Loa Solar Observatory, both located near the mountain's summit. Hawaii Volcanoes National Park covers the summit and the southeastern flank of the volcano, and also incorporates Kīlauea, a separate volcano.
Geology
Setting
Like all Hawaiian volcanoes, Mauna Loa was created as the Pacific tectonic plate moved over the Hawaiian hotspot in the Earth's underlying mantle. The Hawaii island volcanoes are merely the most recent evidence of this process that, over 70 million years, has created the 3,700 mi (6,000 km)-long Hawaiianâ€"Emperor seamount chain. The prevailing view states that the hotspot has been largely stationary within the planet's mantle for much, if not all of the Cenozoic Era. However, while the Hawaiian plume is well-understood and extensively studied, the nature of hotspots themselves remains fairly enigmatic.
Mauna Loa is one of five subaerial volcanoes that make up the island of HawaiÊ»i, created by the Hawaii hotspot. The oldest volcano on the island, Kohala, is more than a million years old, and KÄ«lauea, the youngest, is believed to be between 300,000 and 600,000 years of age. LÅÊ»ihi Seamount on the island's flank is even younger, but has yet to breach the surface. At 1 million to 700,000 years of age, Mauna Loa is the second youngest of the five volcanoes on the lsland, making it the third youngest volcano in the Hawaiian â€" Emperor seamount chain, a chain of shield volcanoes and seamounts extending from Hawaii to the Kurilâ€"Kamchatka Trench in Russia.
Following the pattern of Hawaiian volcanics, Mauna Loa would have started out as young submarine volcano, gradually building itself up through subsurface eruptions of alkali basalt before emerging from the sea through a series of surtseyan eruptions about 400,000 years ago. Since then the volcano has remained active, generating a continual stream of effusive and explosive eruptions, including 33 historical ones since the first well-documented eruption in 1843. Although Mauna Loa's activity has been overshadowed in recent years by that of its neighbor KÄ«lauea, it remains active.
Structure
Mauna Loa is the largest subaerial and second largest overall volcano in the world (behind Tamu Massif), covering a land area of 5,271 km2 (2,035 sq mi) and spans a maximum width of 120 km (75 mi). Consisting of approximately 65,000 to 80,000 km3 (15,600 to 19,200 cu mi) of solid rock, it makes up more than half of the surface area of the island of Hawaiʻi. Combining the volcano's extensive submarine flanks (5,000 m (16,400 ft) to the sea floor) and 4,170 m (13,680 ft) subaerial height, Mauna Loa rises an impressive 9,170 m (30,085 ft) from base to peak, greater than the 8,848 m or 29,029 ft elevation of Mount Everest from sea level to its peak. In addition, much of the mountain is invisible even underwater: its mass depresses the crust beneath it by another 8 km (5 mi), in the shape of an inverse mountain, meaning the true height of Mauna Loa from the start of its eruptive history is about 17,170 m (56,000 ft).
Mauna Loa is a typical shield volcano in form, taking the shape of a long, broad dome extending down to the ocean floor whose slopes are about 12° at their steepest, a consequence of its extremely fluid lava. The shield-stage lavas that built the enormous main mass of the mountain are tholeiitic basalts, like those of Mauna Kea, created through the mixing of primary magma and subducted oceanic crust. Mauna Loa's summit hosts three overlapping pit craters arranged northeast-southwest, the first and last roughly 1 km (0.6 mi) in diameter and the second an oblong 4.2 km × 2.5 km (2.6 mi × 1.6 mi) feature; together these three craters make up the 6.2 by 2.5 km (3.9 by 1.6 mi) summit caldera MokuÊ»Äweoweo, so named for the Hawaiian Ê»Äweoweo fish (Priacanthus meeki), purportedly due to the resemblance of its eruptive fires to the coloration of the fish. MokuÊ»Äweoweo's caldera floor lies between 170 and 50 m (558 and 164 ft) beneath its rim and it is only the latest of several calderas that have formed and reformed over the volcano's life. It was created between 1,000 and 1,500 years ago by a large eruption from Mauna Loa's northeast rift zone, which emptied out a shallow magma chamber beneath the summit and collapsed it into its present form. Additionally, two smaller pit craters lie southwest of the caldera, named Lua Hou (New Pit) and Lua Hohonu (Deep Pit).
Mauna Loa's summit is also the focal point for its two prominent rift zones, marked on the surface by well-preserved, relatively recent lava flows (easily seen in satellite imagery) and linearly arranged fracture lines intersected by cinder and splatter cones. These rift zones are deeply set structures, driven by dike intrusions along a decollement fault that is believed to reach down all the way to the volcano's base, 12 to 14 km (7 to 9 mi) deep. The first is a 60 km (37 mi) rift trending southwest from the caldera to the sea and a further 40 km (25 mi) underwater, with a prominent 40° directional change along its length; this rift zone is historically active across most of its length. The second, northeastern rift zone extends towards Hilo and is historically active across only the first 20 km (12 mi) of its length, with a nearly straight and, in its latter sections, poorly defined trend. The northeastern rift zone takes the form of a succession of cinder cones, the most prominent of which the 60 m (197 ft) high Puu Ulaula, or Red Hill. There is also a less definite northward rift zone that extends towards the Humuula Saddle marking the intersection of Mauna Loa and Mauna Kea.
Simplified geophysical models of Mauna Loa's magma chamber have been constructed, using interferometric synthetic aperture radar measures of ground deformation due to the slow buildup of lava under the volcano's surface. These models predict a 1.1 km (1 mi) wide magma chamber located at a depth of about 4.7 km (3 mi), 0.5 km (0 mi) below sea level, near the southeastern margin of MokuÊ»Äweoweo. This shallow magma chamber is significantly higher-placed than Mauna Loa's rift zones, suggesting magma intrusion into the deeper and occasional dike injections into the shallower parts of the rift zone drive rift activity; a similar mechanism has been proposed for neighboring KÄ«lauea. Earlier models based on Mauna Loa's two most recent eruptions made a similar prediction, placing the chamber at 3 km (1.9 mi) deep in roughly the same geographic position.
Mauna Loa has complex interactions with its neighbors, HualÄlai to the west, Mauna Kea to the north, and particularly KÄ«lauea to the east. Lavas from Mauna Kea intersect with Mauna Loa's basal flows as a consequence of Kea's older age, and Mauna Kea's original rift zones were buried beneath post-shield volcanism from Mauna Loa; additionally, Mauna Kea shares Mauna Loa's gravity well, depressing the ocean crust beneath it by 6Â km (4Â mi). There are also a series of normal faults on Mauna Loa's northern and western slopes, between its two major rift zones, that are believed to be the result of combined circumferential tension from the two rift zones and from added pressure due to the westward growth of neighboring KÄ«lauea.
Because Kīlauea lacks a topographical prominence and appears as a bulge on the southeastern flank of Mauna Loa, it was historically interpreted by both native Hawaiians and early geologists to be an active satellite of Mauna Loa. However, analysis of the chemical composition of lavas from the two volcanoes show that they have separate magma chambers, and are thus distinct. Nonetheless, their proximity has led to a historical trend in which high activity at one volcano roughly coincides with low activity at the other. When Kīlauea lay dormant between 1934 and 1952, Mauna Loa became active, and when the latter remained quiet from 1952 to 1974, the reverse was true. This is not always the case; the 1984 eruption of Mauna Loa started during an eruption at Kīlauea, but had no discernible effect on the Kīlauea eruption, and the ongoing inflation of Mauna Loa's summit, indicative of a future eruption, began the same day as new lava flows at Kīlauea's Puʻu ŌʻŠcrater. Geologists have suggested that "pulses" of magma entering Mauna Loa's deeper magma system may have increased pressure inside Kīlauea and triggered the concurrent eruptions.
Mauna Loa is slumping eastward along its southwestern rift zone, leveraging its mass into KÄ«lauea and driving the latter eastward at a rate of about 10Â cm (4Â in) per year; the interaction between the two volcanoes in this manner has generated a number of large earthquakes in the past, and has resulted in a significant area of debris off of KÄ«lauea's seaward flank known as the Hilina Slump. A system of older faults exists on the southeastern side of Mauna Loa that likely formed before Kilauea became large enough to impede Mauna Loa's slump, the lowest and northernmost of which, the Kaoiki fault, remains an active earthquake center today. The west side of Mauna Loa, meanwhile, is unimpeded in movement, and indeed is believed to have undergone a massive slump collapse between 100,000 and 200,000 years ago, the residue from which, consisting of a scattering of debris up to several kilometers wide and up to 50Â km (31Â mi) distant, is still visible today. The damage was so extensive that the headwall of the damage likely intersected its southwestern rift zone. There is very little movement there today, a consequence of the volcano's geometry.
Mauna Loa is tall enough to have experienced glaciation during the last ice age, 25,000 to 15,000 years ago. Unlike Mauna Kea, on which extensive evidence of glaciation remains even today, Mauna Loa was at the time and has remained active, having grown an additional 150 to 300Â m (492 to 984Â ft) in height since then and covering any glacial deposits beneath new flows; strata of that age doesn't occur until at least 2,000Â m (6,562Â ft) down from the volcano's summit, too low for glacial growth. Mauna Loa also lacks its neighbor's summit permafrost region, although sporadic ice persists in places. It is speculated that extensive phreatomagmatic activity occurred during this time, contributing extensively to ash deposits on the summit.
Eruptive history
Prehistoric eruptions
To have reached its enormous size within its relatively short (geologically speaking) 600,000 to 1,000,000 years of life, Mauna Loa would logically have had to have grown extremely rapidly through its developmental history, and extensive charcoal-based radiocarbon dating (perhaps the most extensive such prehistorical eruptive dating on Earth) has amassed a record of almost two hundred reliably dated extant flows confirming this hypothesis.
The oldest exposed flows on Mauna Loa are thought to be the Ninole Hills on its southern flank, subaerial basalt rock dating back approximately 100 to 200 thousand years. They form a terrace against which younger flows have since banked, heavily eroded and incised against its slope in terms of direction; this is believed to be the result of a period of erosion because of a change in the direction of lava flow caused by the volcano's prehistoric slump. These are followed by two units of lava flows separated by an intervening ash layer known as the PÄhala ash layer: the older Kahuka basalt, sparsely exposed on the lower southwest rift, and the younger and far more widespread KaÊ»u basalt, which appear more widely on the volcano. The PÄhala ashes themselves were produced over a long period of time circa 13 to 30 thousand years ago, although heavy vitrification and interactions with post and pre- creation flows has hindered exact dating. Their age roughly corresponding with the glaciation of Mauna Loa during the last ice age, raising the distinct possibility that it is the product of phreatomagmatic interaction between the long-gone glaciers and Mauna Loa's eruptive activities.
Studies have shown that a cycle occurs in which volcanic activity at the summit is dominant for several hundred years, after which activity shifts to the rift zones for several more centuries, and then back to the summit again. Two cycles have been clearly identified, each lasting 1,500â€"2,000 years. This cyclical behavior is unique to Mauna Loa among the Hawaiian volcanoes. Between about 7,000 and 6,000 years ago Mauna Loa was largely inactive. The cause of this cessation in activity is not known, and no known similar hiatus has been found at other Hawaiian volcanoes except for those currently in the post-shield stage. Between 11,000 and 8,000 years ago, activity was more intense than it is today. However, Mauna Loa's overall rate of growth has probably begun to slow over the last 100,000 years, and the volcano may in fact be nearing the end of its tholeiitic basalt shield-building phase.
Recent history
Ancient Hawaiians have been present on Hawaiʻi island for about 1,500 years, but they preserved almost no records on volcanic activity on the island beyond a few fragmentary accounts dating to the late 18th and early 19th centuries. Possible eruptions occurred around 1730 and 1750 and sometime during 1780 and 1803. A June 1832 eruption was witnessed by a missionary on Maui, but the 190 km (118 mi) between the two islands and lack of apparent geological evidence have cast this testimony in doubt. Thus the first entirely confirmed historically witnessed eruption was a January 1843 event, since which Mauna Loa has erupted anew 32 times.
Historical eruptions at Mauna Loa are typically Hawaiian in character and rarely violent, starting with the emergence of lava fountains over a several kilometer long rift colloquially known as the "curtain of fire" (often, but not always, propagating from Mauna Loa's summit) and eventually concentrating at a single vent, its long-term eruptive center. Activity centered on its summit are usually followed by flank eruptions up to a few months distant, and although Mauna Loa is historically less active than that of its neighbor Kilauea, it tends to produce greater volumes of lava over shorter periods of time. Most eruptions are centered at either the summit or either of its two major rift zones; within the last two hundred years, 38 percent of eruptions occurred at the summit, 31 percent at the northeast rift zone, 25 percent at the southwest rift zone, and the remaining 6 percent from northwest vents. 40 percent of the volcano's surface consists of lavas less than a thousand years old, and 98 percent of lavas less than 10,000 years old. In addition to the summit and rift zones, Mauna Loa's northwestern flank has also been the source of three historical eruptions.
The 1843 event was followed by eruptions in 1849, 1851, 1852, and 1855, with the 1855 flows being particularly extensive. 1859 marked the largest of the three historical flows that have been centered on Mauna Loa's northwestern flank, producing a long lava flow that reached the ocean on Hawaii island's west coast, north of Kiholo Bay. An eruption in 1868 occurred alongside the enormous 1868 Hawaii earthquake, a magnitude eight event that claimed 77 lives and remains the largest earthquake ever to hit the island. Following further activity in 1871, Mauna Loa experienced nearly continuous activity from August 1872 through 1877, a long-lasting and voluminous eruption lasting approximately 1,200 days and never moving beyond its summit. A short single-day eruption in 1877 was unusual in that it took place underwater, in Kealakekua Bay and within a mile of the shoreline; curious onlookers approaching the area in boats reported unusually turbulent water and occasional floating blocks of hardened lava. Further eruptions occurred in 1879 and then twice in 1880, the latter of which extended into 1881 and came within the present boundaries of the island's largest city, Hilo; however at the time the settlement was a shore-side village located further down the volcano's slope, and so was unaffected.
Mauna Loa continued its activity, and of the eruptions that occurred in 1887, 1892, 1896, 1899, 1903 (twice), 1907, 1914, 1916, 1919, and 1926, three (in 1887, 1919, and 1926) were partially subaerial. The 1926 eruption in particular is noteworthy for having inundated of a village near Hoopuloa, destroying 12 houses, a church, and a small harbor. After an event in 1933, Mauna Loa's 1935 eruption caused a public crisis when its flows started to head towards Hilo. A bombing operation was decided upon to try and divert the flows, planned out by then-lieutenant colonel George S. Patton. The bombing, conducted on December 27, was declared a success by Thomas A. Jaggar, director of the Hawaiian Volcano Observatory, and lava stopped flowing by January 2, 1936. However, the role the bombing played in ending the eruption has since been heavily disputed by volcanologists. A longer but summit-bound event in 1940 was comparatively less interesting.
Mauna Loa's 1942 eruption occurred only four months after the attack on Pearl Harbor and United States entry into World War II, and created a unique problem for the wartime United States. Occurring during an enforced nighttime blackout on the island, the eruption's luminosity forced the government to issue a gag order on the local press, hoping to prevent news of its occurrence spreading for fear that the Japanese would use it to launch a bombing run on the island. However, as flows from the eruption rapidly spread down the volcano's flank and threatened the ʻOlaʻa flume, Mountain View's primary water source, the United States Air Force decided to drop its own bombs on the island in the hopes of redirecting the flows away from the flume; sixteen bombs weighing between 300 and 600 lb (136 and 272 kg) each were dropped on the island, but produced little effect. Eventually the eruption ceased on its own.
Following a 1949 event the next major eruption at Mauna Loa occurred in 1950. Originating from the volcano's southwestern rift zone, the eruption remains the largest rift event in the volcano's modern history, lasting 23 days, emitting 376 million cubic meters of lava, and reaching 24 km (15 mi) out to the ocean within 3 hours. The 1950 eruption was not the most voluminous eruption on the volcano (the long-lived 1872-1877 event produced more than twice as much material) but it was easily one of the fastest-acting, producing the same amount of lava as the 1859 eruption in a tenth of the time. Flows overtook the village of Hoʻokena-mauka in South Kona, crossed Hawaii Route 11, and reached the sea within four hours of eruption, and although there was no loss of life the village was permanently destroyed. After the 1950 event Mauna Loa entered an extended period of dormancy, interrupted only by a small single-day summit event in 1975. However it rumbled to life again in 1984, manifesting first at Mauna Loa's summit and then producing a narrow, channelized 'a'a flow that advanced downslope to within 6 km (4 mi) of Hilo, close enough to illuminate the city at nighttime. However the flow got no closer, as two natural levees further up its pathway consequently broke and diverted active flows.
Mauna Loa has not erupted since, and as of January 2013 has remained quiet for nearly 29 years, its longest period of quiet in recorded history.
Hazards
Mauna Loa has been designated a Decade Volcano, one of the sixteen volcanoes identified by the International Association of Volcanology and Chemistry of the Earth's Interior (IAVCEI) as being worthy of particular study in light of their history of large, destructive eruptions and proximity to populated areas. The United States Geological Survey maintains a hazard zone mapping of the island done on a one to nine scale, with the most dangerous areas corresponding the smallest numbers. Based on this classification Mauna Loa's continuously active summit caldera and rift zones have been given a level one designation. Much of the area immediately surrounding the rift zones is considered level two, and about 20 percent of the area has been covered in lava in historical times. Much of the remainder of the volcano is hazard level three, about 15 to 20 percent of which has been covered by flows within the last 750 years. However, two sections of the volcano, the first in the Naalehu area and the second on the southeastern flank of Mauna Loa's rift zone, are protected from eruptive activity by local topography, and have thus been designated hazard level 6, comparable with a similarly isolated segment on KÄ«lauea.
Although volcanic eruptions in HawaiÊ»i rarely produce casualties (the only direct historical fatality due to volcanic activity on the island occurred at KÄ«lauea in 1924, when an unusually explosive eruption hurled rocks at an onlooker), property damage due to inundation by lava is a common and costly hazard. Hawaiian-type eruptions usually produce extremely slow-moving flows that advance at walking pace, presenting little danger to human life, but this is not strictly the case; Mauna Loa's 1950 eruption emitted as much lava in three weeks as KÄ«lauea's current eruption produces in three years and reached sea level within four hours of its start, overrunning the village of HoÊ»okena Mauka and a major highway on the way there. An earlier eruption in 1926 overran the village of HoÊ»ÅpÅ«loa Makai, and Hilo, partly built on lavas from the 1880-81 eruption, is at risk from future eruptions. The 1984 eruption nearly reached the city, but stopped short after the flow was redirected upstream.
A potentially greater hazard at Mauna Loa is a sudden, massive collapse of the volcano's flanks, like the one that struck the volcano's west flank between 100,000 and 200,000 years ago and formed the present-day Kealakekua Bay. Deep fault lines are a common feature on Hawaiian volcanoes, allowing large portions of their flanks to gradually slide downwards and forming structures like the Hilina Slump and the ancient Ninole Hills; large earthquakes could trigger rapid flank collapses along these lines, creating massive landslides and possibly triggering equally large tsunamis. Undersea surveys have revealed numerous landslides along the Hawaiian chain and evidence of two such giant tsunami events: 200,000 years ago, MolokaÊ»i experienced a 75 m (246 ft) tsunami, and 100,000 years ago a megatsunami 325 m (1,066 ft) high struck LÄnaÊ»i. A more recent example of the risks associated with slumps occurred when in 1975 the Hilina Slump suddenly lurched forward several meters, triggering a magnitude 7.2 earthquake and a small tsunami that killed two campers at Halape.
Monitoring
Established on KÄ«lauea in 1912, the Hawaiian Volcano Observatory (HVO), presently a branch of the United States Geological Survey, is the primary organization associated with the monitoring, observance, and study of Hawaiian volcanoes. Thomas A. Jaggar, the observatory's founder, attempted a summit expedition to the volcano to observe its 1914 eruption, but was rebuffed by the arduous trek required (see Ascents). After soliciting help from Lorrin A. Thurston, in 1915 he was able to persuade the US Army to construct a "simple route to the summit" for public and scientific use, a project completed in December of that year; the Observatory has maintained a presence on the volcano ever since.
Eruptions on Mauna Loa are almost always preceded and accompanied by prolonged episodes of seismic activity, the monitoring of which was the primary and often only warning mechanism in the past and which remains viable today. Seismic stations have been maintained on Hawaiʻi since the Observatory's inception, but these were concentrated primarily on Kīlauea, with coverage on Mauna Loa improving only slowly through the 20th century. Following the invention of modern monitoring equipment, the backbone of the present-day monitoring system was installed on the volcano in the 1970s. Mauna Loa's July 1975 eruption was forewarned by more than a year of seismic unrest, with the HVO issuing warnings to the general public from late 1974; the 1984 eruption was similarly preceded by as much as three years of unusually high seismic activity, with volcanologists predicting an eruption within two years in 1983.
The modern monitoring system on Mauna Loa is constituted not only by its locally seismic network but also of a large number of GPS stations, tiltmeters, and strainmeters that have been anchored on the volcano to monitor ground deformation due to swelling in Mauna Loa's subterranean magma chamber, which presents a more complete picture of the events proceeding eruptive activity. The GPS network is the most durable and wide-ranging of the three systems, while the tiltmeters provide the most sensitive predictive data, but are prone to erroneous results unrelated to actual ground deformation; nonetheless a survey line across the caldera measured a 76 mm (3 in) increase in its width over the year preceding the 1975 eruption, and a similar increase in 1984 eruption. Strainmeters, by contrast, are relatively rare. The Observatory also maintains two gas detectors at MokuÊ»Äweoweo, Mauna Loa's summit caldera, as well as a publicly accessible live webcam and occasional screenings by interferometric synthetic aperture radar imaging.
Human history
Pre-contact
The first Ancient Hawaiians to arrive on Hawaii island lived along the shores where food and water were plentiful. Flightless birds that had previously known no predators became a staple food source. Early settlements had a major impact on the local ecosystem, and caused many extinctions, particularly amongst bird species, as well as introducing foreign plants and animals and increasing erosion rates. The prevailing lowland forest ecosystem was transformed from forest to grassland; some of this change was caused by the use of fire, but the main reason appears to have been the introduction of the Polynesian Rat (Rattus exulans).
Ancient Hawaiian religious practice holds that the five volcanic peaks of the island are sacred, and regards Mauna Loa, the largest of them all, with great admiration; but what mythology survives today consists mainly of oral accounts from the 18th century first compiled in the 19th. Most of these stories agree that the Hawaiian volcano deity, Pele, resides in HalemaÊ»umaÊ»u Crater on Kilauea; however a few place her home at Mauna Lao's summit caldera MokuÊ»Äweoweo, and the mythos in general associates her with all volcanic activity on the island. Regardless, KÄ«lauea's lack of a geographic outline and strong volcanic link to Mauna Loa led to it being considered an offshoot of Mauna Loa by the Ancient Hawaiians, meaning much of the mythos now associated with KÄ«lauea was originally directed at Mauna Loa proper as well.
Ancient Hawaiians constructed an extensive trail system on HawaiÊ»i island, today known as the Ala Kahakai National Historic Trail. The network consisted of short trailheads servicing local areas along the main roads and more extensive networks within and around agricultural centers. The positioning of the trails were practical, connecting living areas to farms and ports and regions to resources, with a few upland sections reserved for gathering and most lines marked well enough to remain identifiable long after regular use has ended. One of these trails, the Ainapo Trail, ascended from the village of KapÄpala over 3,400 m (11,155 ft) in about 56 km (35 mi) and ended at MokuÊ»Äweoweo at Mauna Loa's summit. Although the journey was arduous and required several days and many porters, ancient Hawaiians likely made the journey during eruptions to leave offerings and prayers to honor Pele, much as they did at HalemaÊ»umaÊ»u, neighboring Kilauea's more active and more easily accessible caldera. Several camps established along the way supplied water and food for travelers.
European summiting attempts
James Cook's third voyage was the first to make landfall on HawaiÊ»i island, in 1778, and following adventures along the North American west coast Cook returned to the island in 1779. On his second visit John Ledyard, a corporal of the Royal Marines aboard the HMS Resolution, proposed and receiving approval for an expedition to summit Mauna Loa to learn "about that part of the island, particularly the peak, the tip of which is generally covered with snow, and had excited great curiosity." Using a compass, Ledyard and small group of ships' mates and native attendants attempted to make a direct course for the summit. However on the second day of traveling the route became steeper, rougher, and blocked by "impenetrable thickets," and the group was forced to abandon their attempt and return to Kealakekua Bay, reckoning they had "penetrated 24 miles and we suppose [were] within 11 miles of the peak"; in reality, MokuÊ»Äweoweo lies only 32 km (20 mi) east of the bay, a severe overestimation on Ledyard's part. Another of Cook's men, Lieutenant James King, estimated the peak to be at least 5,600 m (18,373 ft) high based on its snow line.
The next attempt to summit Mauna Loa was an expedition led by Archibald Menzies, a botanist and naturalist on the 1793 Vancouver Expedition. In February of that year Menzies, two ships' mates, and a small group of native Hawaiian attendants attempted a direct course for the summit from Kealakekua Bay, making it 26Â km (16Â mi) inland by their reckoning (an overestimation) before they were turned away by the thickness of the forest. On a second visit by the expedition to the island in January of the next year Menzies was placed in charge of exploring the island interior, and after traversing the flanks of HualÄlai he and his party arrived at the high plateau separating the two volcanoes. Menzies decided to make a second attempt (above the objections of the accompanying island chief), but again his progress was arrested by unassailable thickets.
Menzies made a third attempt to summit Mauna Loa in February of 1794. This time the botanist consulted King Kamehameha I for advice and learned that he could take canoes to the south and follow the Ê»AinapÅ Trail, not knowing of its existence beforehand. Significantly better prepared, Menzies, Lieutenant Joseph Baker and Midshipman George McKenzie of the Discovery, and a servant (most likely Jonathan Ewins, listed on the ship's muster as "Botanist's L't") reached the summit, which Menzies estimated to be 4,156 m (13,635 ft) high with the aid of a barometer (consistent with a modern value of 4,169 m (13,678 ft)). He was surprised to find heavy snow and morning temperatures of âˆ'3 °C (27 °F), and was unable to compare the heights of Mauna Loa and Kea but correctly supposed the latter to be taller based on its larger snow cap. The feat of summitting Mauna Loa was not to be repeated for forty years.
The Hawaiian Islands were the site of fervent missionary work, with the first group of missionaries arrived at Honolulu in 1820 and the second in 1823. Some of these missionaries left for HawaiÊ»i island, and spent ten weeks traveling around it, preaching at local villages and climbing Kilauea, from which one of its members, William Ellis, observed Mauna Loa with the aid of a telescope and ascertained it and Kea to be "perhaps 15,000 to 16,000 feet above the level of the sea"; they did not, however, attempt to climb the volcano itself. It is sometimes reported that the missionary Joseph Goodrich reached the summit around this time, but he never claimed this himself, though he did summit Mauna Kea and describe MokuÊ»Äweoweo with the aid of another telescope.
The next successful ascent was made on January 29, 1834, 40 years later, by the Scottish botanist David Douglas, who also reached the summit caldera using the ʻAinapŠTrail. By the time Douglas reached the summit the environment had put him under extreme duress, but he nonetheless stayed overnight to make measurements of the summit caldera's proportions and record barometric data on its height, both now known to be widely inaccurate. Douglas collected biological samples on the way both up and down, and after a difficult and distressing descent began collating his samples; he planned to return to England, but instead several months later his body was mysteriously discovered crushed in a pit besides a dead wild boar.
Isidor Löwenstern successfully climbed Mauna Loa in February 1839, only the third successful climb in 60 years.
Wilkes expedition
The United States Exploring Expedition led by Lieutenant Charles Wilkes was tasked with a vast survey of the Pacific Ocean starting in 1838. In September 1840 they arrived in Honolulu, where repairs to the ships took longer than expected. Wilkes decided to spend the winter in Hawaii and take the opportunity to explore its volcanoes while waiting for better weather to continue the expedition. King Kamehameha III assigned American medical missionary Dr. Gerrit P. Judd to the expedition as a translator.
Wilkes sailed to Hilo on the island of Hawaiʻi and decided to climb Mauna Loa first, since it looked easier than Mauna Kea. On December 14 he hired about 200 porters, but after he left he realized only about half the equipment had been taken, so he had to hire more Hawaiians at higher pay. When they reached Kīlauea after two days, their guide Puhano headed off to the established ʻAinapŠTrail. Wilkes did not want to head back downhill so he blazed his own way through dense forest directed by a compass. The Hawaiians were offended by the waste of sacred trees which did not help morale. At about 6,000 feet (1,800 m) elevation they established a camp called "Sunday Station" at the edge of the forest.
Two guides joined them at Sunday Station: Keaweehu, "the bird-catcher" and another whose Hawaiian name is not recorded, called "ragsdale". Although Wilkes thought he was almost to the summit, the guides knew they were less than half way up. Since there was no water at Sunday Station, porters had to be sent back ten miles (16 km) to a lava tube on ʻAinapŠTrail which had a known supply. After an entire day replenishing stocks, they continued up to a second camp they called "Recruiting Station" at about 9,000 feet (2,700 m) elevation. After another full day's hike they established "Flag Station" on December 22, and by this time were on the ʻAinapŠTrail. Most of the porters were sent back down to get another load.
At the Flag Station Wilkes and his eight remaining men built a circular wall of lava rocks and covered the shelter with a canvas tent. A snowstorm was in progress and several suffered from altitude sickness. That night (December 23), the snow on the canvas roof caused it to collapse. At daylight some of the group went down the trail to retrieve firewood and the gear abandoned on the trail the day before. After another day's climb, nine men reached the rim of MokuÊ»Äweoweo. They could not find a way down its steep sides so chose a smooth place on the rim for the camp site, at coordinates 19°27′59″N 155°34′54″W. Their tent was pitched within 60 feet (18 m) of the crater's edge, secured by lava blocks.
The next morning they were unable to start a fire using friction due to the thin air at that altitude, and sent for matches. By this time, the naval officers and Hawaiians could not agree on terms to continue hiring porters, so sailors and marines were ordered from the ships. Dr. Judd traveled between the summit and the Recruiting Station to tend the many who suffered from altitude sickness or had worn out their shoes on the rough rock. Christmas Day was spent building rock walls around the camp to give some protection from the high winds and blowing snow. It took another week to bring all the equipment to the summit, including a pendulum designed for measuring slight variations in gravity.
On December 31, 1840 the pre-fabricated pendulum house was assembled. Axes and chisels cut away the rock surface for the pendulum's base. It took another three days to adjust the clock to the point where the experiments could begin. However, the high winds made so much noise that the ticks could often not be heard, and varied the temperature to make measurements inaccurate. Grass had to be painstakingly brought from the lowest elevations for insulation to get accurate measurements.
On Monday, January 11, Wilkes hiked around the summit crater. Using an optical method, he estimated Mauna Kea was only 193 feet (59Â m) higher (modern measurements are 104 feet (32Â m)). On January 13, 1841, he had "Pendulum Peak, January 1841 U.S. Ex, Ex." cut into a rock at the site. The tents were dismantled and Hawaiians carried the gear down over the next three days, while Wilkes enjoyed a lomilomi Hawaiian massage. He continued his measurements at lower elevations and left the island on March 5. For all the effort he did not obtain any significant results, attributing gravity discrepancies to "the tides".
The Wilkes expedition's camp site's ruins are the only known physical evidence in the Pacific of the U. S. Exploring Expedition. The camp site was listed on the National Register of Historic Places on July 24, 1974 as site 74000295, and is state historic site 10-52-5507.
Today
A summit shelter was built with some of the stones from Wilkes' camp site and mortar in 1934. In 1916 MokuÊ»Äweoweo was included in Hawaii Volcanoes National Park, and a new trail was built directly from park headquarters at KÄ«lauea, an even more direct route than the one taken by Wilkes. This trail, arriving at the summit from the east via Red Hill, became the preferred route due to its easier access and gentler slope. The historic Ê»AinapÅ Trail fell into disuse, and was reopened in the 1990s. A third modern route to the summit is from the Saddle Road up to the Mauna Loa Observatory which is at 11,135 feet (3,394 m) elevation a few miles north of MokuÊ»Äweoweo and the North Pit trail.
Climate
Trade winds blow from east to west across the Hawaiian islands, and the presence of Mauna Loa strongly affects the local climate. At low elevations, the eastern (windward) side of the volcano receives heavy rain; the city of Hilo is the wettest in the United States. The rainfall supports extensive forestation. The western (leeward) side has a much drier climate. At higher elevations, the amount of precipitation decreases, and skies are very often clear. Very low temperatures mean that precipitation often occurs in the form of snow, and the summit of Mauna Loa is described as a periglacial region, where freezing and thawing play a significant role in shaping the landscape.
Mauna Loa has a tropical climate with warm temperatures at lower elevations and cool to cold temperatures higher up year-round. Below is the table for the slope observatory, which is at 10,000 feet (3,000 m) in the alpine zone. The highest recorded temperature was 85 °F (29 °C) and the lowest was 18 °F (âˆ'8 °C) on February 18, 2003 and February 20, 1962, respectively.
Observatories
The location of Mauna Loa has made it an important location for atmospheric monitoring by the Global Atmosphere Watch and other scientific observations. The Mauna Loa Solar Observatory (MLSO), located at 11,155 feet (3,400Â m) on the northern slope of the mountain, has long been prominent in observations of the Sun. The NOAA Mauna Loa Observatory (MLO) is located close by. From its location well above local human-generated influences, the MLO monitors the global atmosphere, including the greenhouse gas carbon dioxide. Measurements are adjusted to account for local outgassing of CO2 from the volcano.
The Yuan-Tseh Lee Array for Microwave Background Anisotropy (AMiBA) sits at an elevation of 11,155 feet (3,400Â m). It was established in October 2006 by the Academia Sinica Institute of Astronomy and Astrophysics (ASIAA) to examine cosmic microwave background radiation.
See also
- Outline of Hawaii
- Index of Hawaii-related articles
- Evolution of Hawaiian volcanoes
- List of Ultras in Oceania
- List of Ultras in the United States
- Mountain peaks of Hawaii
- Table of the major 4000 meter summits of the United States
References
External links
- United States Geological Survey
- Hawaii Center for Volcanology
- Global Volcanism Program entry
- Mauna Loa Observatory (MLO) â€" NOAA
- Mauna Loa Solar Observatory (MLSO)
- 1934 USGS silent color video of Mauna Loa erupting
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