Atmospheric Temperature Variation after the 1991 Mt. Pinatubo Eruption

Kawamata, Masahiro; Yamadal, Shingo; Kudoh, Tatsuya; Takano, Kiyoharu; Kusunoki, Shoji

doi:10.2151/jmsj1965.70.6_1161

Cited by 9 publications

(5 citation statements)

References 5 publications

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“…Global lower stratospheric (30-100 hPa) temperature anomalies increased after the eruption, and global tropospheric (300-850 hPa) temperature anomalies decreased after the eruption in spite of the warm ENSO episode in 1991/1992 (Kawamata et al, 1992). Global tropospheric temperatures generally increase after a warm ENSO episode.…”

Section: Introductionmentioning

confidence: 97%

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

et al. 2012

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Section: Introductionmentioning

confidence: 97%

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

et al. 2012

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“…Global lower stratospheric (30-100 hPa) temperature anomalies increased after the eruption, and global tropospheric (300-850 hPa) temperature O. Uchino et al: On recent (2008 stratospheric aerosols observed by lidar over Japan anomalies decreased after the eruption in spite of the warm ENSO episode in 1991/1992 (Kawamata et al, 1992). Global tropospheric temperatures generally increase after a warm ENSO episode.…”

Section: Introductionmentioning

confidence: 99%

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

Uchino¹,

Sakai²,

Nagai³

et al. 2012

Preprint

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Abstract. An increase in stratospheric aerosols caused by the volcanic eruption of Mt. Nabro (13.37° N, 41.70° E) on 12 June 2011 was first detected by lidar at Tsukuba (36.05° N, 140.13° E) and Saga (33.24° N, 130.29° E) in Japan. The maximum backscattering ratios at a wavelength of 532 nm were 2.0 at 17.0 km on 10 July 2011 at Tsukuba and 3.6 at 18.2 km on 23 June 2011 at Saga. The maximum integrated backscattering coefficients (IBCs) above the first tropopause height were 4.18 × 10−4 sr−1 on 11 February 2012 at Tsukuba and 4.19 × 10−4 sr−1 on 23 June 2011 at Saga, respectively. A time series of lidar observational results at Tsukuba have also been reported from January 2008 through May 2012. Increases in stratospheric aerosols were observed after the volcanic eruptions of Mt. Kasatochi (52.18° N, 175.51° E) in August 2008 and Mt. Sarychev Peak (48.09° N, 153.20° E) in June 2009. The yearly averaged IBCs at Tsukuba were 2.60 × 10−4 sr−1, 2.52 × 10−4 sr−1, 2.45 × 10−4 sr−1, and 2.20 × 10−4 sr−1 for 2008, 2009, 2010, and 2011, respectively. These values were about twice the IBC background level (1.21 × 10−4 sr−1) from 1997 to 2001 at Tsukuba. We briefly discuss the influence of the increased aerosols on climate and the implications for analysis of satellite data.

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“…If there is a pronounced phenomenon such as El Niñ o or La Niñ a, the direct cause of the abnormal weather is attempted to link with them using the analysis of quasi-stationary Rossby wave-train (Bell and Halpert 1998;Bell et al 1999;Kushnir et al 2002;Peng et al 2003). If there is a major volcanic eruption, the abnormal weather is attempted to explain with them by the analysis of radiative impact to the atmosphere (Kawamata et al 1992;Graf et al 1994). However, if there is no such obvious impact of external forcing on the atmosphere, the abnormal weather would be elucidated as a natural variability contained in the chaotic nonlinear fluid mechanics, and the true direct and indirect causes are something of an enigma (see Namias 1978;Branstator 1990;Yasunari 1997;Frederiksen and Branstator 2001;Kravtsov et al 2003;Branstator and Frederiksen 2003;Tanaka 2003a).…”

Section: Introductionmentioning

confidence: 99%

Analysis of Recent Extreme Events Measured by the Barotropic Component of the Atmosphere

Tanaka¹,

Matsueda

2004

Journal of the Meteorological Society of Japan

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In this study, recent extreme events over the Northern Hemisphere are quantified in terms of an energy norm of the anomaly of the state variables. Since persistent low-frequency variabilities are characterized, in most cases, by their barotropic structure, the energy norm of the anomaly is measured for the barotropic component of the atmosphere. The norm is then normalized by its climatology to assess the abnormality of the extreme events. In this study the norm is evaluated in the framework of the 3-D spectral primitive equation model to assess the external forcing as well as the state variabiles.According to the analysis of the monthly mean anomaly data for 50 years from 1953 to 2002, the most abnormal months appear to be Apr. 1997, Jan. 1963, Jan. 1977, Mar. 1983, Apr. 1967, Feb. 1989, and Jan. 1989. Those are well known abnormal months in the past studies. In this study, the top 3% of the extreme events are listed as the abnormal months.The quantification of the abnormality is further extended to the external forcing of the barotropic component of the atmosphere and also to the SST anomaly. It is found that only 3 cases of the abnormal months (Jan. 1963, Feb. 1989 and Jan. 1989 are associated with the abnormal external forcing, and the rest of the abnormal months are associated with the non-abnormal external forcing. Likewise, it is found that most of the abnormal external forcing result in a non-abnormal month. The SST forcing anomaly is not directly related to the external forcing. It is concluded from the result that more than 80% of the abnormal months are induced by the natural variability of the barotropic component of the atmosphere under the non-abnormal external forcing for the last 50 years. For the monthly time scale, the chaotic nonlinear behavior is quantitatively larger than a linear response to the external forcing or that to the SST anomaly.

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Atmospheric Temperature Variation after the 1991 Mt. Pinatubo Eruption

Cited by 9 publications

References 5 publications

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

On recent (2008–2012) stratospheric aerosols observed by lidar over Japan

Analysis of Recent Extreme Events Measured by the Barotropic Component of the Atmosphere

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