On Volcanic and Other Particulate Turbidlty Anomalies

Deirmendjian, D.

doi:10.1016/s0065-2687(08)60353-2

Cited by 66 publications

(39 citation statements)

References 26 publications

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“…direction on the horizon, it rose towards its zenith in the form of a cone, [and] shone with a This phenomenon, known as a twilight glow, typically follows in the aftermath of strong volcanic eruptions (e.g. observations reported in with the prolonged afterglow caused by light scattering from stratospheric aerosols (Deirmendjian, 1973). These dates coincide with those mentioned by Francisco José de Caldas for the upper atmospheric veil in Colombia, suggesting that the same aerosol cloud was responsible for the sunset after-glow described by Hipólito Unanue in Peru.…”

Section: Resultsmentioning

confidence: 99%

“…Stothers and Rampino, 1983;Stothers, 1999) and vivid sunset glows Lamb, 1970;Deirmendjian, 1973). The haze is caused by concentrated layers of volcanic aerosols, within the troposphere or stratosphere depending on the altitude where the sulfate aerosols are injected, and can become widely dispersed (Stothers, 1999).…”

Section: A Guevara-murua Et Al: Observations Of a Stratospheric Aermentioning

confidence: 99%

“…Perhaps the most common atmospheric disturbances described following large explosive eruptions are vivid sunsets, and in particular a prolonged twilight after-glow due to the enhanced forward scattering caused by the volcanic aerosols in the stratosphere Deirmendjian, 1973). This phenomenon has been observed worldwide after recent major volcanic eruptions and reported in contemporary documents following historic events such as Awu (Indonesia, 1641), Katla (Iceland, 1660), Laki (Iceland, 1783), Tambora (Indonesia, 1815) and Krakatau (Indonesia, 1883) (e.g.…”

Section: A Guevara-murua Et Al: Observations Of a Stratospheric Aermentioning

confidence: 99%

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Observations of a stratospheric aerosol veil from a tropical volcanic eruption in December 1808: is this the Unknown ∼1809 eruption?

et al. 2014

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Section: Resultsmentioning

confidence: 99%

Section: A Guevara-murua Et Al: Observations Of a Stratospheric Aermentioning

confidence: 99%

Section: A Guevara-murua Et Al: Observations Of a Stratospheric Aermentioning

confidence: 99%

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Observations of a stratospheric aerosol veil from a tropical volcanic eruption in December 1808: is this the Unknown ∼1809 eruption?

et al. 2014

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“…added between 16 and 30 million tons of aerosols to the stratosphere (Deirmendjian, 1973;Cadle et al, , 1977. In April 1982, Mexico's El Chichón added between 10 and 20 million tons of aerosol (Hofmann and Rosen, 1983;McCormick and Swissler, 1983;Mroz et al, 1983).…”

Section: Interannual Variability In Irradiance and Sunshine Durationmentioning

confidence: 99%

Solar radiation climate change over southern Africa and an assessment of the radiative impact of volcanic eruptions

Power

Mills²

2005

Int. J. Climatol.

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Spatial and temporal variability in global, diffuse, and horizontal direct irradiance and sunshine duration has been evaluated at eight stations in South Africa and two stations in Namibia where the time series range between 21 and 41 years. Global and direct irradiance and sunshine duration decrease from northwest to southeast; diffuse irradiance increases toward the east. Annually averaged global irradiance G a decreased between 1.3% (2.8 W m −2 ) and 1.7% (4.4 W m −2 ) per decade at Bloemfontein, Cape Town, Durban, Pretoria, and Upington. Annually averaged diffuse irradiance D a decreased 5.2% (3.0 W m −2 ) per decade at Grootfontein and 4.2% (3.1 W m −2 ) per decade at Port Elizabeth. Annual direct irradiance B a decreased 2.1% (3.5 W m −2 ) per decade at Cape Town and 2.8% (5.7 W m −2 ) per decade at Alexander Bay. A simultaneous decrease in annually averaged daily sunshine duration S a may have contributed to the decrease in B a at Alexander Bay and the decrease in G a at Pretoria. Increases in aerosols may have contributed to the observed decrease in G a at Cape Town and Durban, and the decrease in D a at Grootfontein may be due to a decrease in aerosols. On average, variability in S a explains 89.0%, 50.4%, and 89.5% of the variance in G a , D a , and B a respectively. The radiative response to changes in sunshine duration is greater for direct irradiance than for global and diffuse. In the 2 years following the 1963 Mount Agung eruption in Indonesia, changes in global irradiance over southern Africa were small and inconsistent. At eight stations, diffuse irradiance increased 21.9% (13.3 W m −2 ) on average and direct irradiance decreased 8.7% (15.5 W m −2 ). After the 1982 El Chichón eruption in Mexico, global irradiance increased at two stations and decreased at seven stations. Eight stations witnessed an increase in diffuse irradiance averaging 7.2% (4.0 W m −2 ) and a decrease in direct irradiance of 5.0% (9.0 W m −2 ). The contribution of changes in cloud cover to the observed changes in irradiances appears to be small. Following the 1991 Mount Pinatubo eruption in the Philippines, diffuse irradiance increased an average of 18.8% (10.0 W m −2 ) at three stations and direct irradiance decreased by 7.2% (13.0 W m −2 ).

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“…The Agung eruption occurred before the advent of satellite-based measurements of atmospheric aerosols and SO 2, although early ground-based lidar and other optical instruments were making measurements of atmospheric turbidity at that time (Fiocco and Grams 1964;Voltz 1970;Deirmendjian 1973). However, an estimate of the mass of stratospheric H 2 SO 4 aerosols emitted during the 1963 Agung eruption can be made from stratospheric aerosol optical depth, a measure of the degree of opacity of the stratosphere to sunlight transmission.…”

Section: Estimate Of Volatile Emissions From Optical Depth Measurementsmentioning

confidence: 99%

Petrology and sulfur and chlorine emissions of the 1963 eruption of Gunung Agung, Bali, Indonesia

Self

King

1996

Bulletin of Volcanology

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The 1963 eruption of Gunung Agung produced 0.95 km 3 dense rock equivalent (DRE) of olivineBhornblende-bearing, weakly phyric, basaltic andesite tephra and lava. Evidence for magma mixing in the eruptive products includes whole-rock compatible and incompatible trace element trends, reverse and complex compositional zoning of mineral phases, disequilibrium mineral assemblages, sieve-textured plagioclase phenocrysts, and augite rims on reversely zoned orthopyroxene. Basalt magma mixed with pre-existing andesite magma shortly before eruption to yield basaltic andesite with a temperature of 1040-1100 7C at an assumed pressure of 2 kb, f O 2`N NO, and an average melt volatile content (H 2 OBCO 2 ) of 4.3 wt.%. Magmamixing end members may have provided some of the S and Cl emitted in the eruption. Glass inclusions in phenocrysts contain an average of 650 ppm S and 3130 ppm Cl as compared with 70 ppm and 2220 ppm, respectively, in the matrix glass. Maximum S and Cl contents of glass inclusions approach 1800 and 5000 ppm, respectively. Application of the petrologic method to products of the 1963 eruption for estimating volatile release yields of 2.5!10 12 g (Mt) of SO 2 and 3.4 Mt of Cl released from the 0.65 km 3 of juvenile tephra which contributed to stratospheric injection of H 2 SO 4 aerosols on 17 March and 16 May, when eruption column heights exceeded 20 km above sea level. An independent estimate of SO 2 release from atmospheric aerosol loading (11)(12) suggests that approximately 7 Mt of SO 2 was injected into the stratosphere. The difference between the two estimates can be most readily accounted for by the partitioning of S, as well as some Cl, from the magma into a water-rich vapor phase which was released upon eruption. For other recent high-S-release eruptions of more evolved and oxidized magmas (El Chichón, Pinatubo), the petrologic method gives values two orders of magnitude less than independent estimates of SO 2 emissions. Results from this study of the Agung 1963 magma and its volatile emissions, and from related studies on eruptions of more mafic magmas, suggest that SO 2 emissions from eruptions of higher-Ssolubility magma may be more reliably estimated by the petrologic method than may those from moreevolved magma eruptions.

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On Volcanic and Other Particulate Turbidlty Anomalies

Cited by 66 publications

References 26 publications

Observations of a stratospheric aerosol <i>veil</i> from a tropical volcanic eruption in December 1808: is this the <i>Unknown</i> ∼1809 eruption?

Observations of a stratospheric aerosol <i>veil</i> from a tropical volcanic eruption in December 1808: is this the <i>Unknown</i> ∼1809 eruption?

Solar radiation climate change over southern Africa and an assessment of the radiative impact of volcanic eruptions

Petrology and sulfur and chlorine emissions of the 1963 eruption of Gunung Agung, Bali, Indonesia

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On Volcanic and Other Particulate Turbidlty Anomalies

Cited by 66 publications

References 26 publications

Observations of a stratospheric aerosol &lt;i&gt;veil&lt;/i&gt; from a tropical volcanic eruption in December 1808: is this the &lt;i&gt;Unknown&lt;/i&gt; ∼1809 eruption?

Observations of a stratospheric aerosol &lt;i&gt;veil&lt;/i&gt; from a tropical volcanic eruption in December 1808: is this the &lt;i&gt;Unknown&lt;/i&gt; ∼1809 eruption?

Solar radiation climate change over southern Africa and an assessment of the radiative impact of volcanic eruptions

Petrology and sulfur and chlorine emissions of the 1963 eruption of Gunung Agung, Bali, Indonesia

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Observations of a stratospheric aerosol <i>veil</i> from a tropical volcanic eruption in December 1808: is this the <i>Unknown</i> ∼1809 eruption?

Observations of a stratospheric aerosol <i>veil</i> from a tropical volcanic eruption in December 1808: is this the <i>Unknown</i> ∼1809 eruption?