Academic literature on the topic 'Eruption, 1805'

Abstract. The Unknown eruption of 1808/1809 was the second most explosive SO2-rich volcanic eruption in the last two centuries, eclipsed only by the cataclysmic VEI 7 Tambora eruption in April 1815. However, no eyewitness accounts of the event, and therefore its location, or the atmospheric optical effects associated with its aerosols have been documented from historical records. Here we report on two meteorological observations dating from the end of 1808 that describe phenomena we attribute to volcanic-induced atmospheric effects caused by the Unknown eruption. The observations were made by two highly respected Latin American scientists. The first, Francisco José de Caldas, describes a stratospheric aerosol haze, a "transparent cloud that obstructs the sun's brilliance", that was visible over the city of Bogotá, Colombia, from 11 December 1808 to at least mid-February 1809. The second, made by physician José Hipólito Unanue in Lima, Peru, describes sunset after-glows (akin to well-documented examples known to be caused by stratospheric volcanic aerosols) from mid-December 1808 to February 1809. These two accounts provide direct evidence of a persistent stratospheric aerosol veil that spanned at least 2600 km into both Northern and Southern Hemispheres and establish that the source was a tropical volcano. Moreover, these observations confirm that the Unknown eruption, previously identified and tentatively assigned to February 1809 (±4 months) from analysis of ice core sulfate records, occurred in late November or early December 1808 (4 December 1808 ±7 days). This date has important implications for the associated hemispheric climate impacts and temporal pattern of aerosol dispersal.

Abstract. The "Unknown" eruption of 1808/1809 was the second most explosive SO2-rich volcanic eruption in the last two centuries, only eclipsed by the cataclysmic VEI 7 Tambora eruption in April 1815. However, no eyewitness accounts of the event, and therefore its location, or the atmospheric optical effects associated with its aerosols have been documented from historical records. Here we report on two meteorological observations dating from the end of 1808 that describe phenomena we attribute to volcanic-induced atmospheric effects caused by the Unknown eruption. The observations were made by two highly respected Latin American scientists. The first, Francisco José de Caldas, describes a stratospheric aerosol haze, a "transparent cloud that obstructs the sun's brilliance", that was visible over the city of Bogotá, Colombia, from 11 December 1808 to at least mid-February 1809. The second, made by physician José Hipólito Unanue in Lima, Peru, describes sunset after-glows (akin to well-documented examples known to be caused by stratospheric volcanic aerosols) from mid-December 1808 to February 1809. These two accounts provide direct evidence of a persistent stratospheric aerosol veil that spanned at least 2600 km into both Northern and Southern Hemispheres and establish that the source was a tropical volcano. Moreover, these observations confirm that the Unknown eruption, previously identified and tentatively assigned to February 1809 (±4 months) from analysis of ice core sulphate records, occurred in late November or early December 1808 (4 December 1808 ± 7 days). This date has important implications for the associated hemispheric climate impacts and temporal pattern of aerosol dispersal.

AbstractCareful mineral and structural analyses have revealed the characteristics of volcanic ash in the nine horizons of an 80.2 m ice core from Collins Ice Cap, King George Island, Antarctica.Under the assumption of steady state, the Dansgaard-Johnsen flow model was employed to date the core. The volcanic eruptive sequence established for the South Shetland Islands region since AD 1650 shows seven volcanic eruptive cycles during the past 340 years covered by the ice core. It seems that during the period 1875-1925 there was frequent volcanic activity, with perhaps many eruptions at Deception Island. The years 1650-1800 appear to have been a quiet period, followed by a more turbulent century. The past century is basically a tranquil era except for two turbulent epochs at the beginning of the century and in the 1950s-70s.Many of the volcanic eruptions in the ice-core sequence are found in the previously reported records for this region. The few that are not in the records should be further investigated. The absence of any 1967-70 eruption trace in the core suggests that this period may represent a minimum in volcanic activity.

Global Navigation Satellite Systems have been extensively used to investigate the ionosphere response to various natural and man-made phenomena for the last three decades. However, ionospheric reaction to volcano eruptions is still insufficiently studied and understood. In this work we analyzed the ionospheric response to the 11–16 June 2009 VEI class 4 Sarychev Peak volcano eruption by using surrounding Russian and Japanese GPS networks. Prominent covolcanictotal electron content (TEC)ionospheric disturbances (CVIDs) with amplitudes and periods ranged between 0.03–0.15 TECU and 2.5–4.5 min were discovered for the three eruptive events occurred at 18:51 UT, 14 June; at 01:15 and 09:18 UT, 15 June 2009. The estimates of apparent CVIDs velocities vary within 700–1000 m/s in the far-field zone (300–900 km to the southwest from the volcano) and 1300–1800 m/s in close proximity toSarychev Peak. The characteristics of the observed TEC variations allow us to attribute them to acoustic mode. The south-southwestward direction is preferred for CVIDs propagation. We concluded that the ionospheric response to a volcano eruption is mainly determined by a ratio between explosion strength and background ionization level. Some evidence of secondary (F2-layer) CVIDs’ source eccentric location were obtained.

Abstract. The “1809 eruption” is one of the most recent unidentified volcanic eruptions with a global climate impact. Even though the eruption ranks as the third largest since 1500 with a sulfur emission strength estimated to be 2 times that of the 1991 eruption of Pinatubo, not much is known of it from historic sources. Based on a compilation of instrumental and reconstructed temperature time series, we show here that tropical temperatures show a significant drop in response to the ∼ 1809 eruption that is similar to that produced by the Mt. Tambora eruption in 1815, while the response of Northern Hemisphere (NH) boreal summer temperature is spatially heterogeneous. We test the sensitivity of the climate response simulated by the MPI Earth system model to a range of volcanic forcing estimates constructed using estimated volcanic stratospheric sulfur injections (VSSIs) and uncertainties from ice-core records. Three of the forcing reconstructions represent a tropical eruption with an approximately symmetric hemispheric aerosol spread but different forcing magnitudes, while a fourth reflects a hemispherically asymmetric scenario without volcanic forcing in the NH extratropics. Observed and reconstructed post-volcanic surface NH summer temperature anomalies lie within the range of all the scenario simulations. Therefore, assuming the model climate sensitivity is correct, the VSSI estimate is accurate within the uncertainty bounds. Comparison of observed and simulated tropical temperature anomalies suggests that the most likely VSSI for the 1809 eruption would be somewhere between 12 and 19 Tg of sulfur. Model results show that NH large-scale climate modes are sensitive to both volcanic forcing strength and its spatial structure. While spatial correlations between the N-TREND NH temperature reconstruction and the model simulations are weak in terms of the ensemble-mean model results, individual model simulations show good correlation over North America and Europe, suggesting the spatial heterogeneity of the 1810 cooling could be due to internal climate variability.

Non Small Cell Lung Cancer(NSCLC) is the most common type of Lung Cancer. It is characterized by multiple mutations, the commonest being the EGFR and KRAS. Afatinib is an immaculate drug used in Non-Small Cell Lung Cancer, with EGFR mutations. Here we are presenting a case of a 70 year old male, with Non-Small Cell Lung Carcinoma, started on Afatinib, who subsequently developed multiple raised skin lesions over the face, neck and the upper chest. On examination, multiple crusted papules and pustules over the face and anterior chest were present. A diagnosis of Photo distributed Acneiform Eruption secondary to Afatinib was made. Patient was treated appropriately and lesions subsided with post inflammatory hyperpigmentation.This article highlights the characteristic Afatinib induced papulo – pustular eruptions, which eventually responded to treatment.

AbstractDuring the past 220 years, prominent signals of non-sea salt sulfate ion (nssSO42–) concentration exceeding the background level, including both marine biogenic and anthropogenic SO42–, were found in shallow ice cores from site H15 in East Antarctica and Site-J in southern Greenland. They were mostly correlated with past explosive volcanic eruptions. on the basis of this result and published results of shallow ice cores and snow pits at various locations on the Antarctic and Greenland ice sheets, eight common signals were found, of which six were assigned to the following explosive eruptions: El Chichόn, Mexico, in 1982; Agung, Indonesia, in 1963; Santa Maria, Guatemala, in 1902; Krakatau, Indonesia, in 1883; Cosiguina, Nicaragua, in 1835; an unknown volcano between 1831 and 1834; Tambora, Indonesia, in 1815; and an unknown volcano in 1809. Volcanic eruptions which have a potential to imprint their signals in both the Antarctic and Greenland ice sheets were characterized by (1) location in low latitudes between 20˚N and 10˚ S, and (2) eruption column height ≥25 km, corresponding to a volcanic explosivity index (VEI) ≥5.

Abstract. The eruption of Mount Tambora in Indonesia in 1815 was one of the most powerful of its kind in recorded history. This contribution addresses climatic responses to it, the post-eruption weather, and its impacts on human life in the Czech Lands. The climatic effects are evaluated in terms of air temperature and precipitation on the basis of long-term homogenised series from the Prague-Klementinum and Brno meteorological stations, and mean Czech series in the short term (1810–1820) and long term (1800–2010). This analysis is complemented by other climatic and environmental data derived from rich documentary evidence. Czech documentary sources make no direct mention of the Tambora eruption, neither do they relate any particular weather phenomena to it, but they record an extremely wet summer for 1815 and an extremely cold summer for 1816 (the "Year Without a Summer") that contributed to bad grain harvests and widespread grain price increases in 1817. Possible reasons for the cold summers in the first decade of the 19th century reflected in the contemporary press included comets, sunspot activity, long-term cooling and finally – as late as 1817 – earthquakes with volcanic eruptions.

Sea-rafted Loisels Pumice is one of the few stratigraphic markers used to correlate late Holocene coastal deposits in New Zealand. Along with underlying sea-rafted products of the local Taupo eruption of ca. 1800 yr B.P., these events have been used to bracket the first arrival of humans at New Zealand. Loisels Pumice is dacitic to rhyolitic (SiO2 63–78 wt%) in composition, but individual clasts are homogeneous (SiO2 range ± 1 wt%). Characteristics include very low K2O (0.5–1.75 wt%) and Rb (<25 ppm) and a mineralogy dominated by calcic and mafic xenocrysts. Similar features are shared by pumices of the Tonga–Kermadec arc, suggesting a common tholeiitic oceanic source. Interclast diversity of Loisels Pumice suggests that it is the product of several eruptive events from different volcanoes. The differences in glass and mineral compositions found at various sites can be explained if the deposits are from different events. A multisource origin can also partially explain the discrepancy in reported 14C ages (ca. 1500–600 yr B.P.) from different localities. Therefore, the value of Loisels Pumice as a stratigraphic marker is questionable, and it does not constrain the arrival of humans. The predominant westward drift of historic Tonga–Kermadec arc pumices and prevailing ocean currents suggest a long anticlockwise semicircular transport route into the Tasman Sea before sea-rafted pumice arrival in New Zealand. The diversity of the pumices indicates that silicic eruptions frequently occur from the predominantly basic oceanic volcanoes.

Abstract. The aim of this work is to elucidate the impact of changes in solar irradiance and energetic particles vs. volcanic eruptions on tropospheric global climate during the Dalton Minimum (DM, 1780–1840 AD). Separate variations in the (i) solar irradiance in the UV-C with wavelengths λ < 250 nm, (ii) irradiance at wavelengths λ > 250 nm, (iii) in energetic particle spectrum, and (iv) volcanic aerosol forcing were analyzed separately, and (v) in combination, by means of small ensemble calculations using a coupled atmosphere-ocean chemistry-climate-model. Global and hemispheric mean surface temperatures show a significant dependence on solar irradiance at λ > 250 nm. Also, powerful volcanic eruptions in 1809, 1815, 1831 and 1835 significantly decrease global mean temperature by up to 0.5 K for 2–3 yr after the eruption. However, while the volcanic effect is clearly discernible in the southern hemispheric mean temperature, it is less significant in the Northern Hemisphere, partly because the two largest volcanic eruptions occurred in the SH tropics and during seasons when the aerosols were mainly transported southward, partly because of the higher northern internal variability. In the simulation including all forcings, temperatures are in reasonable agreement with the tree-ring-based temperature anomalies of the Northern Hemisphere. Interestingly, the model suggests that solar irradiance changes at λ < 250 nm and in energetic particle spectra have only insignificant impact on the climate during the Dalton Minimum. This downscales the importance of top-down processes (stemming from changes at λ < 250 nm) relative to bottom-up processes (from λ > 250 nm). Reduction of irradiance at λ > 250 nm leads to a significant (up to 2%) decrease of the ocean heat content (OHC) between the 0 and 300 m of depth, whereas the changes in irradiance at λ < 250 nm or in energetic particle have virtually no effect. Also, volcanic aerosol yields a very strong response, reducing the OHC of the upper ocean by up to 1.5%. In the simulation with all forcings, the OHC of the uppermost levels recovers after 8–15 yr after volcanic eruption, while the solar signal and the different volcanic eruptions dominate the OHC changes in the deeper ocean and prevent its recovery during the DM. Finally, the simulations suggest that the volcanic eruptions during the DM had a significant impact on the precipitation patterns caused by a widening of the Hadley cell and a shift of the intertropical convergence zone.

In 1815, Tambora volcano produced one of the largest and deadliest explosive eruptions in the last 1000 years. What if this eruption were to happen today in the modern World? The grain size distribution of distal Tambora ash has been investigated on land and in the deep sea. Deep sea ash layers are well preserved and even the finest ash particles «10 microns) are present, which is particularly important as many volcanoes are located in vicinity of the sea. An improved atmospheric gravity current sedimentation model is presented, able to reproduce the measured grain size distribution and model the ash dispersal of the eruption, while taking into account the ash depositing once the eruption ceases. Ash thicknesses of these samples and from historical documentations were used to estimate eruption volumes. A number of methods combined estimate a volume of 45±5 km3 DRE, divided into 25±3 km3 DRE ash fall and 20±3 km3 DRE pyroclastic flow material. The ash fall is further divided into 10±3 Plinian, and 15±3 km3 DRE co-ignimbrite ash. A colder, drier climate is modelled after the eruption, influencing the carbon cycle by increasing plant productivity (NPP). Atmospheric C02 gets removed while about 13 Gt carbon is taken up mainly by tropical soil reservoirs. C3 and C4 plants, here an analogy for crops, show that C3 productivity increases, while reduced C4 productivity potentially leads to negative C4 crop yields. The same eruption in a future climate would result in lower N-American temperature anomalies in contrast to the past eruption, likely due to a higher pressure region bringing cold Arctic air onto the continent, and a larger sea-ice extent anomaly increasing the albedo in this region. Regionally, more extreme (positive and negative) precipitation anomalies are found , as well as larger negative temperature anomalies.

El sistema de centros eruptivos de flanco de la erupción de 1835 A.D. del volcán Osorno (SCEFVO-1835), se encuentra ubicado en el flanco SW del volcán, presenta una distribución espacial de orientación general NNE-SSW y está constituído por una veintena de conos piroclásticos y cráteres secos, además de cuatro fisuras eruptivas que se habrían originado en dicho episodio eruptivo. En el presente trabajo se estudian, a escala local, parámetros geológicos, geomorfológicos y estructurales de este sistema, con el objetivo de inferir las condiciones tectónicas imperantes durante el episodio que lo originó evaluando las hipótesis vigentes sobre el origen y significado de las erupciones de flanco en estratovolcanes, particularmente en la Zona Volcánica Sur (ZVS). La mayoría de las erupciones de flanco sobre estratovolcanes están relacionadas con un drenaje lateral de magma desde el conducto central a través de diques radiales, cuya propagación es producto de fracturamiento hidráulico. Con la premisa de que los diques alimentadores verticales se propagan ortogonalmente al mínimo esfuerzo tectónico horizontal, se analizan los conos de flanco en estratovolcanes como indicadores de paleo-esfuerzos tectónicos. Cuando el campo regional de esfuerzos es intenso en regímenes de rumbo, la orientación del alineamiento de centros eruptivos de flanco es relativamente lineal y paralela al esfuerzo máximo horizontal (SHmax), con un alto ángulo respecto de la tendencia general del frente volcánico principal. Con la finalidad de inferir la disposición de los diques alimentadores, además de los alineamientos de conos, se realizan mediciones directas de las fisuras eruptivas junto a otros parámetros morfológicos de los conos tales como las elongaciones del cráter y su base y la orientación de depresiones en el borde del cráter. Mientras que a escala regional el volcán Osorno forma parte de un cordón volcánico de orientación NE-SW, interpretado previamente como un dominio extensional del arco volcánico, controlado a su vez por un régimen transpresivo en el Cuaternario; a escala del edificio volcánico, los centros eruptivos de flanco se distribuyen de manera menos regular dando cuenta, probablemente, de otros procesos. En este sentido, se estudian fenómenos locales que pueden afectar la disposición de los diques, como la reorientación que sufrirían producto de la carga gravitacional del edificio principal. Se concluye que tanto el alineamiento de conos como la orientación de fisuras eruptivas, reflejan efectivamente la disposición de un sistema de fracturas alimentadoras, neoformadas en el sustrato volcánico. Estas fracturas, que dan origen al SCEFVO-1835, formarían parte de un sistema extensivo, de orientación NE-SW, relacionado con el régimen general transpresivo dextral, siendo éste el mecanismo de control predominante sobre el ascenso y extrusión de magmas durante este evento eruptivo. A escala local, en zonas elevadas y de pendiente más pronunciada, se sugiere la sobreimposición del esfuerzo gravitacional local en la propagación de las fracturas alimentadoras.

Postglacial activity on the Askja volcanic system, north Iceland, has been dominated by basaltic volcanism. Over 80% of Askja's postglacial basalts fall within a relatively narrow compositional range containing between 4 and 8 wt.% MgO. The 'main series' is further divided into two groups separated by a distinct compositional gap evident in major and trace element concentrations. The most evolved basalts formed by fractional crystallisation within shallow magma reservoirs, followed by the extraction of residual liquid from a semi-rigid, interconnected crystal network. This process is analogous to the formation of melt segregations within single lava flows, and was responsible for generating several small-volume, aphyric basaltic lavas erupted along caldera ring fractures surrounding the Oskjuvatn (Askja lake) caldera in the early 20th century. Further examples of evolved basalt are found throughout Askja's postglacial volcanic record. However, Askja's early postglacial output is dominated by more primitive compositions. Some of the most primitive basalts erupted within the Askja caldera are found in phreatomagmatic tuff cone sequences which crop out in the walls of Oskjuvatn caldera. one such tuff sequence has been dated at between 2.9 and 3.6 ka. This tuff cone shares geochemical source characteristics, such as Nb/La and Nb/Zr, with basaltic tephras erupted during precursory activity to the Plinian-phreatoplinian eruption of 28th-29th March 1875. It may therefore be considered to be compositionally representative of the primitive basaltic magmas supplied to Askja during the postglacial period. The predominance of relatively primitive basalt (6.8 wt.% MgO) within Askia's postglacial lava succession suggests that it did not have a permanent shallow magma chamber during the postglacial period. It is envisaged that the postglacial Askja magmas evolved by a process of polybaric factionation in transient, sill-like magma storage zones located at various levels in the crust. The most primitive magmas erupted directly from deeper reservoirs, while the more evolved magmas experienced longer crustal residence times. The buoyant rise of volatile-enriched melt from these sill-like bodies, without mobilising phenocryst phases, explains the observation that almost all lavas on Askja's eastern and southern lava aprons are essentially aphyric. The 28th-29th March 1975 eruption marked the climax of a volcanotectonic episode on the Askja volanic system lasting from late 1874 to early 1876. Fissure eruptions also occurred at the Sveinagja graben, 45-65 km north of Askja, between February and October 1875, producing the Nyjahraun lava. A strong similarity exists between whole-rock major element concentrations from Myjahraun and the Askja 20th century basalts. This has led to the suggestion that these basalts originated from a common shallow magma reservoir beneath Askja central volcano, with the Nyjahraun eruptions being fed by a lateral dyke extending northwards from Askja. This theory also offers an explanation for the observation that the volume of phyolitic ejecta from 28th-29th March 1875 is significantly less than the volume of Oskjuvatn caldera, which was formed as a result of this eruption. New major and trace element data from whole-rock and glass samples indicated that Nyjahraun and the Askja 20th century basalts did not share a common parental magma. A detailed investigation of historical accounts from explorers and scientists who visited Askja between 1875 and 1932 reveals that Oskjuvatn caldera took over 40 years to reach its current form, and that its size in 1876 was equal to the volume erupted on 28th-29th March 1875. Small injections of magma into an igneous intrusion complex beneath Askja, coupled with background deflation, are sufficient to provide the required accommodation space for continued caldera collapse after 1876. Lateral flow is therefore not required to explain the volume of Oskjuvatn caldera, nor the eruption of evolved basaltic magma on the Askja volcanic system in 1875. It has been conjectured that the Holuhraun lava, located at the southern tip of the Askja volcanic system, was also connected with the 1874-76 Askja volcanotectonic episode. However, major and trace element data from whole-rock samples, glass and melt inclusions receal the Holuhraun is geochemically more similar to basalts erupted on the Bardarbunga-Veidivotn volcanic system than to postglacial basalts from Askja. The division between the 'Askja' and 'Veidivotn' geochemical signatures appears to be linked to east-west-striking lineations in the region south of Askja. This indicates that a particular geochemical signature is not necessarily confined to the tectonic expression of a single volcanic system, and has important implications for the identification and delineation of individual volcanic systems beneath the northwest sector of Vatnajokull.

Purpose: To retrospectively assess the incidence and predictive factors for self-correction of ectopic eruption of maxillary permanent first molars (EE) and the prevailing attitudes amongst surveyed specialists regarding intervention in cases of EE. Methods: Charts of patients diagnosed with EE were assessed for predictive clinical and radiographic factors. An online survey was sent to pediatric dentists and orthodontists. Results: The rate of self-correction was 71%. One third of self-corrections occurred after age 9. Increased amount of impaction (r(43)=0.59, p<.001) and degree of resorption (r(57)=0.41, p=.001) were positively correlated with irreversibility. Orthodontists estimated the spontaneous self-correction rate to be lower (t(1178)=19.2, p<.001) than pediatric dentists. Conclusions: One third of self-corrections occurred after 9 years of age and delaying treatment of EE may be a viable option when uncertain of the outcome. Reliable predictive factors of irreversibility of EE were identified. Differences exist between pediatric dentists and orthodontists regarding management of EE.

The bulk of the eruption of Askja in north central Iceland on March 28-29 1875 consisted of a plinian eruption that lasted 6-7 hours, produced 0.2 km3 of ash and rhyolitic pumice, and created a surge and partially welded ash/pumice fall deposit that crops out on the shore of the modern caldera lake (Sparks et al. 1981). We evaluate the volatile budget of the magma during the eruption and focus on water concentration in glass fragments and shards, glass adjacent to crystals, and melt inclusions (MIs). Sparks et al. (1981) estimated the gas exit velocity at the vent was 380 m/s during the plinian phase, and the water concentration at 2.8 wt%. Measurements of water concentration in basaltic and rhyolitic glass shards from layers C through E range from 0.15 to 0.5 wt%, with variations within layers, a drop in layer D, and increase in layer E. Plagioclase and pyroxene crystals from layers C through E contain rhyolitic MIs with water concentrations ranging from 0.1 to 1.8 wt%, some higher than the matrix glass. Magma underwent degassing on its way to the surface. Rhyolitic glass adjacent to crystals hosting MIs has the highest water concentration, from 0.4 to 2.18 wt%. This, and the initial phreatoplinian eruptive style, both suggest interaction of magma with meteoric water during the eruption. Intimate mixtures of basaltic glass compositions within samples and basaltic glass surrounded by rhyolitic glass support the conclusion of Sigurdsson and Sparks (1981) that magmas mingled prior to and during the eruption.

‘The Enemy Within’ begins with volcanic super-eruptions and their devastating consequences such as the 1815 eruption of volcano Tambora in Indonesia, and ancient eruptions in Yellowstone, USA, and Toba, northern Sumatra. Volcanic explositivity index, eruption magnitude, and eruption intensity are explained. Volcanic landslides in Hawaii and the Canary Islands will, in the future, result in giant tsunamis wreaking havoc around the Pacific and Atlantic Ocean rims. But when will they happen? Finally, the fate of industrial cities, such as Tokyo, located near active fault-lines and in earthquake zone, and the resultant effects on the world economy are considered.

In order to classify volcanic eruptions and their potential effects on the atmosphere, Newhall and Self (1982) proposed a scale of explosive magnitude, the Volcanic Explosivity Index (VEI), based mainly on the volume of the erupted products (and the height of the volcanic eruption column). VEI’s range varies from VEI = 0 (for strictly non-explosive eruptions) to VEI = 8 (for explosive eruptions producing ∼1012 m3 bulk volume of tephra). Eruption rates for VEI = 8 eruptions may be greater than 106 m3s−1 (Ninkovich et al., 1978a, 1978b). Eruptions also differ in the amounts of sulphur-rich gases released to form stratospheric aerosols. Therefore, the sulphur content of the magma, the efficiency of degassing, and the heights reached by the eruption column are important factors in the climatic effects of eruptions (Palais and Sigurdsson, 1989; Rampino and Self, 1984). Historic eruptions of VEI ranging from three to six (volume of ejecta from <1 km3 to a few tens of km3) have produced stratospheric aerosol clouds up to a few tens of Mt. These eruptions, including Tambora 1815 and Krakatau 1883, have caused cooling of the Earth’s global climate of a few tenths of a degree Centigrade (Rampino and Self, 1984). The most recent example is the Pinatubo (Philippines) eruption of 1991 (Graf et al., 1993; Hansen et al., 1996). Volcanic super-eruptions are defined as eruptions that are tens to hundreds of times larger than historic eruptions, attaining a VEI of 8 (Mason et al., 2004; Rampino, 2002; Rampino et al., 1988; Sparks et al., 2005). Super-eruptions are usually caldera-forming events and more than twenty super-eruption sites for the last 2 million years have been identified in North America, South America, Italy, Indonesia, the Philippines, Japan, Kamchatka, and New Zealand. No doubt additional super-eruption sites for the last few million years exist (Sparks et al., 2005). The Late Pleistocene eruption of Toba in Sumatra, Indonesia was one of the greatest known volcanic events in the geologic record (Ninkovich et al., 1978a, 1978b; Rampino and Self, 1993a; Rose and Chesner, 1990).

The Reconstruction era embraces the twelve years, from 1865 to 1877, of active effort to rebuild and reconstitute the American union after the attempt by the Confederate States of America to secede from it. The Introduction explains how it left a long legacy of bitterness, especially among Southerners who believed that they had fought an honorable war and were handed a dishonorable peace. Reconstruction also coincided with an eruption of unprecedented levels of graft, corruption, and fraud in American civil governments. But Reconstruction is probably best known, and least liked, for its failure to erase the treacherous impact of slavery and race in a reconstructed and unified nation.

As the Western economy grew and industrialized, society came to rely less directly on agriculture and the vagaries of the seasons. This is illustrated by tracing a series of major climatic disturbances from the late eighteenth century onward and showing how those natural factors lost much of their impact. In the early part of that era, beginning in the 1780s, volcanic eruptions contributed to an alarming era of climate disruption, and the Tambora blast in particular (1815) sparked new churches and denominations teaching apocalyptic and millenarian doctrines, with dreams of the end times. But as we proceed deeper into the nineteenth century, much of Western humanity, at least, felt ever more detached from the direct impact of climate.

In 1816, Against A foreboding climatic background, Mary Shelley wrote Frankenstein. She might well have begun: “It was a dark and stormy decade …” During the previous year, much of the world had been shrouded by the great ashen veil cast across the skies by the massive Tambora volcanic eruption in April 1815. Europe’s 1815– 1816 was a cold, gloomy, and tumultuous time. Crops failed and tem­peratures fell. Bonaparte was consigned to the rocky island of St. Helena, Beethoven entered his more radical and introspective late period, and minor autocratic monarchies around the continent came under increasing political siege as democratic impulses stirred. This chapter examines some of the shorter- term climate shifts and extreme weather events that have occurred over the last two centuries. The disrupted weather following the Tambora eruption, for example, shows how small changes in temperature and rainfall can have major consequences, including failed harvests and epidemic outbreaks. In mid- nineteenth- century Ireland, the failure of the potato crop in wet and relatively warm conditions contributed to food insecurity that devastated the local population. Unusual weather extremes in late- nineteenth- century China, including a period of cooling, facilitated the Third Pandemic of bubonic plague, which spread rapidly through populations already under stress due to harvest failures, conflict, and political turmoil. Such events may intensify in the coming decades as the Earth’s average temperature rises and climatic cycles are disrupted and become more variable. Additionally, the consequences for human population health are amplified by social and political mismanagement and turmoil. We can expect climate change to act as a “force multiplier,” exacerbating many of the world’s health problems. From the mid- nineteenth century, the northern hemisphere’s Little Ice Age receded as solar activity regained its twelfth- century peak level. The depths of the cold had been reached around 1700 C.E., and the cool­ing influence of the Siberian High was now receding. The almost year- round ice and snow in northern Europe during those super- chilled earlier times were long gone, and the snowbound, though increasingly grimy, White Christmases of early- 1800s Dickensian London were waning.

So far, the geographical foci of our regional–thematic examination of the linkages between war and disease have been the great continental land masses of the Americas, Europe, Asia, and Africa. We now turn our attention to a different stage for the geographical spread of war epidemics—oceanic islands. As well as the particular interest which attaches to islands as natural laboratories for the study of epidemiological processes (Cliff et al., 1981, 2000), island epidemics also hold a special place in war history. For example, we saw in Chapter 2 how the islands of the Caribbean became staging posts for the spread of wave upon wave of Old World ‘eruptive fevers’ (especially measles, plague, smallpox, and typhus) brought by the Spanish conquistadores to the Americas during the sixteenth century. Much later, the mysterious fever that broke out on the island of Walcheren in 1809 ranks as one of the greatest medical disasters to have befallen the British Army. In this chapter, we examine the theme of island epidemics with special reference to the military engagements of Australia, New Zealand, and the neighbouring islands of the South Pacific since 1850. Figure 11.1 serves as a location map for the discussion, while sample conflicts—exclusive of tribal feuds, skirmishes, and other minor events for which little or no documentary evidence exists—are listed in Table 11.1. Our analysis begins in Section 11.2. There we provide a brief review of the initial introduction and spread of some of the Old World diseases which occurred in association with South Pacific colonization and conflicts during the last half of the nineteenth century. In Sections 11.3 and 11.4, we move on to the twentieth century. In the Great War, Australia and New Zealand made a relatively larger contribution to military manpower than any other allied country. At the end of the conflict, the return of many tens of thousands of antipodean troops from the battlefields of Europe fuelled the extension of the 1918–19 ‘Spanish’ influenza pandemic into the South Pacific region (Cumpston, 1919). In Section 11.3, we examine the spread of influenza on board returning troopships and subsequently within Australia, New Zealand, and the neighbouring islands of the region.

Negative pressure is one of the metastable states of liquids at which it can be extended up to a certain limit without a gap of continuity. There are numerous experimental studies where a negative pressure up to 40 MPa has been obtained at laboratory conditions. However, these results of the experimental works were not practically implemented, as real liquids both in the nature and the technological processes contain impurities. Under certain kinetic and hydrodynamic conditions the waves of negative pressure in real liquids (crude oil, water, and water-based solutions) were observed. The wave of negative pressure is a turned soliton wave with one negative hump. It is a conservative wave, which maintains its shape and dimensions, and travels long distances with the speed of sound. An advanced technology of generation of the negative pressure wave in real systems allowed creating completely new energy saving technology. This technology based on negative pressure phenomenon has been already used for increasing oil production efficiency during various oil well operations, cleaning of oil well bore, and pipelines from various accumulations. It is shown that a new technology has a lot of potentials for bottom-hole cleaning operations, oil recovery enhancement, pipeline transportation, gas-lift operation etc. Negative pressure is known to be one of the metastable states at which liquids can be extended up to a certain limit. Theoretic evaluations show that in pure liquids negative pressure may reach large values while the liquid may stand significant extending efforts. For instance, the maximum negative pressure that may be sustained by ideally pure water is estimated as −109N/m2. It means that an imaginable rope of completely pure water with the diameter of 0.01m can sustain a huge extending effort more than 105 N. It is evident that the real experimental values of negative pressure are much less than the corresponding theoretic estimations. It is connected with the impossibility of obtaining ideally pure liquids without any “weak places” (gas bubbles, admixture, etc) and with the circumstance that in experience, the rupture often happens not in the liquid volume but on the surface touching the walls of the vessels weakened by the existence of thin films, embryos, etc. There are numerous results of the experimental work of static and dynamic character, where negative pressure has appeared in one or another degree [1]. In laboratory conditions, negative pressure apparently was first revealed in the experiences made by F. M. Donny (1843), who used degassed sulfuric acid and obtained negative pressure only −0.012 MPa. Among the further attempts of receiving bigger negative pressure, it is worth mentioning the experiences made by O.Reynolds, M.Bertelot and J.Meyer. Basing upon a centrifugal method and using mercury, L.J.Briggs obtained the record value of negative pressure (−42.5 MPa). But as a matter of fact, beginning from the first experiences by F. M. Donny, the main condition in the investigations for the appearance of negative pressure has been the homogeneous character of the liquid and high degree of the purity the liquid-vessel system. Significant values of negative pressure has been obtained under those conditions, however these results of a great scientific importance have no effective applications in practice as real liquids in Nature and technological processes are heterogeneous multicomponent systems. A long-term experimental work has been done to generate negative negative pressure in real liquid systems and investigate influence of this state on thermohydrodynamical characteristics of natural and technological processes [2,3]. Basing on the idea that negative pressure can be created due to the sudden character of extending efforts a direct wave of the negative pressure in real liquids (water, oil, solutions etc.) have been obtained experimentally. For impulsive entering into metastable (overheated) zone in a phase diagram “liquid-vapor” the pressure should drop so fast that the existing centers of evaporation (bubbles, embryos, admixtures etc.) would not be able to manifest themselves for this period. In these terms purity of the liquid is not decisive, and herewith there might exist states of an overheated liquid with the manifestation of negative pressure. It was determined that wave of the negative pressure resembling overturned soliton wave with one but negative peak propagates with speed of sound. The typical variation of the pressure in the petroleum stream in pipe is given in Figure 1. Reversed wave of the negative pressure was not recorded during the experiments. Evidently this is associated with considerable structural changes in the liquid after the passing of the direct wave. The arising negative pressure though being a short-term, results in a considerable overheating of the fluid system and leads to spontaneous evaporation and gas-emanation with the further cavitation regime. It was determined that after passing of the negative pressure wave hydraulic resistance in the system becomes much less, and significant increase of permeability of the porous medium and intensification of the filtration process take place. On the base of the investigations it was made a conclusion that any discharge in the hydraulic systems when the drop of the pressure requires much less time that relaxation of the pressure in the system inevitably results in the arising of rarefaction wave, in particular, the negative pressure wave [4]. The larger is the hydraulic system and the higher is the depression of the pressure, the more intensively the negative pressure wave may manifest itself. In certain terms waves of the positive pressure may be reflected from free surfaces, different obstacles, from contact surfaces between phases in the form of the reverse wave of the negative pressure. On this base there were presented numerous theoretical and experimental works on the simulation of the process, investigation of impact of the negative pressure on certain physical features of real systems [5]. The negative pressure wave may lead to very hard complications: showings of oil and gas leading sometimes to dreadful open fountains, borehole wall collapse, column crushing, gryphon appearance [6]. Analysis of numerous facts of complications, troubles in wells as water-oil-gas showings, crushing of columns, collapses, gryphon formation demonstrates that they arise usually as a result of round-trip operations in drilling of wells and their capital repairs. The negative pressure wave may be initiated by a sudden pulling of pipes or drilling equipment, as well as their sudden braking, quick opening of a valve at the well exit, etc, resulting in metastable extension of the working fluid agent. Though impulse negative pressure manifests itself as a significant dynamic factor, its structural consequences are more dangerous for an oil well. Moving along a well the negative pressure wave results in the spontaneous boiling of the water in the drilling fluid, and as a result of considerable reduction of its specific weight the hydrostatic column is “switched-off’ for some seconds and this may be sufficient for oil and gas showings of the well to be appeared accompanied often by crushing of columns and collapsing of wells due to great destroying energy manifestation. Negative pressure waves may be considered also as one of the dominant factors in geophysical processes, especially, in evolution and appearance of volcanic eruptions and earthquakes [7,8]. Extreme dynamic processes in the underground medium as a matter of fact can be considered as a synergetic manifestation of the negative pressure together with other thermohydrodynamical factors. The waves of negative pressure in the underground environment may be initiated by tectonic dislocations and faults as a result of different dynamic processes, dramatic decrease of pressure during the displacement of fluids and rocks. They may arise also in the form of a reverse waves as a result of reflection of ordinary seismic waves from different underground surfaces. On the basis of received results the method of artificial creation of negative pressure waves has been created [4]. The essence of the method is that negative pressure waves can be generated by means of discharge in hydraulic systems (pipes, wells, etc) when the drop of the pressure takes place during the characteristic time much less than that of pressure relaxation in the system. The greater is the volume of hydraulic system and the higher is the depression of the pressure, the more intensively the negative pressure wave may manifest itself. This method was taken as a basis of elaboration of principally new technologies and installations to increase effectiveness and efficiency of some oil recovery processes. It has been worked out and widely tested in field conditions new technologies on using of the negative pressure phenomenon for cleaning of oil producing hydraulic systems/well bore, pipeline/from various accumulations and increasing of effectiveness of oil producing at different well operation methods. The technology provides generation negative pressure waves in the well using the special mechanisms that leads to the shock depression impact upon the oil stratum, and as a result, to considerable growth in the oil influx, bottom-hole cleaning, accompanied by essential saving both reservoir and lifting energies, elimination and prevention of sandy bridging, paraffin, silt, water, etc. accumulations. For implementations of these technologies corresponding installations have been elaborated, in part, equipments for cleaning out of oil holes from sand plugs, increasing of efficiency and effectiveness of gas-lift well operations and bottom-hole pumping. In cleaning out of oil-holes from sand plugs the most operative and effective liquidation of different sand plugs irrespective of their rheological character is provided, associated with complete bottom-hole cleaning, essential increase of oil recovery and overhaul period. Elaborated equipment is simple and easy to use. Other comparatively advantageous application of the technology provides increase of efficiency of a gas-lift well operation, expressed in considerable reduction of a specific gas consumption associated with essential increase of oil recovery and overhaul period. The design of the equipment is reliable and simple to service. There are different modifications of the equipment for single-row, double-row lifts in packer and packerless designs. The introduced technologies have passed broad test in field conditions. The operative and complete cleaning of numerous oil wells was carried out, where the altitude of sand plugs varied from 20m to 180m; oil output of wells and their overhaul period have been increased and specific gas discharge reduced significantly.