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Lava effusion rates from hand-held thermal infrared imagery: an example from the June 2003 effusive activity at Stromboli
Author(s)
Language
English
Obiettivo Specifico
Status
Published
JCR Journal
JCR Journal
Peer review journal
Yes
Title of the book
Issue/vol(year)
/68(2005)
Pages (printed)
107–117
Issued date
2005
Abstract
A safe, easy and rapid method to calculate lava
effusion rates using hand-held thermal image data was developed
during June 2003 at Stromboli Volcano (Italy).We
used a Forward Looking Infrared Radiometer (FLIR) to
obtain images of the active lava flow field on a daily basis
between May 31 and June 16, 2003. During this time
the flow field geometry and size (where flows typically a
few hundred meters long were emplaced on a steep slope)
meant that near-vertical images of the whole flow field
could be captured in a single image obtained from a helicopter
hovering, at an altitude of 750 m and ∼1 km off
shore.We used these images to adapt a thermally based effusion
rate method, previously applied to low and high
spatial resolution satellite data, to allow automated extraction
of effusion rates from the hand-held thermal infrared
imagery. A comparison between a thermally-derived
(0.23–0.87m3 s−1) and dimensionally-derived effusion rate
(0.56 m3 s−1) showed that the thermally-derived range was
centered on the expected value. Over the measurement period,
the mean effusion rate was 0.38±0.25 m3 s−1, which is similar to that obtained during the 1985–86 effusive eruption
and the time-averaged supply rate calculated for normal
(non-effusive) Strombolian activity. A short effusive
pulse, reaching a peak of ∼1.2 m3 s−1, was recorded on
June 3, 2003. One explanation of such a peak would be an
increase in driving pressure due to an increase in the height
of the magma contained in the central column.We estimate
that this pulse would require the magma column to attain a
height of ∼190 m above the effusive vent, which is approximately
the elevation difference between the vent and the
floor of the NE crater. Our approach gives an easy-to-apply
method that has the potential to provide effusion rate time
series with a high temporal resolution.
effusion rates using hand-held thermal image data was developed
during June 2003 at Stromboli Volcano (Italy).We
used a Forward Looking Infrared Radiometer (FLIR) to
obtain images of the active lava flow field on a daily basis
between May 31 and June 16, 2003. During this time
the flow field geometry and size (where flows typically a
few hundred meters long were emplaced on a steep slope)
meant that near-vertical images of the whole flow field
could be captured in a single image obtained from a helicopter
hovering, at an altitude of 750 m and ∼1 km off
shore.We used these images to adapt a thermally based effusion
rate method, previously applied to low and high
spatial resolution satellite data, to allow automated extraction
of effusion rates from the hand-held thermal infrared
imagery. A comparison between a thermally-derived
(0.23–0.87m3 s−1) and dimensionally-derived effusion rate
(0.56 m3 s−1) showed that the thermally-derived range was
centered on the expected value. Over the measurement period,
the mean effusion rate was 0.38±0.25 m3 s−1, which is similar to that obtained during the 1985–86 effusive eruption
and the time-averaged supply rate calculated for normal
(non-effusive) Strombolian activity. A short effusive
pulse, reaching a peak of ∼1.2 m3 s−1, was recorded on
June 3, 2003. One explanation of such a peak would be an
increase in driving pressure due to an increase in the height
of the magma contained in the central column.We estimate
that this pulse would require the magma column to attain a
height of ∼190 m above the effusive vent, which is approximately
the elevation difference between the vent and the
floor of the NE crater. Our approach gives an easy-to-apply
method that has the potential to provide effusion rate time
series with a high temporal resolution.
Sponsors
NSF grant EAR-0207734
United States Geological Survey
Italian Civil Protection
United States Geological Survey
Italian Civil Protection
References
Allard P, Carbonnelle J, Metrich N, Loyer H, Zettwoog P (1994)
Sulphur output and magma degassing budget of Stromboli
volcano. Nature 368:326–330
Calvari S, Neri M, Pinkerton H (2002) Effusion rate estimations
during the 1999 summit eruption on Mount Etna, and growth of
two distinct lava flow fields. J Volcanol Geotherm Res 119:107–
123
Calvari S, Andronico D, Burton MR, Dehn J, Garf`ı G, Harris A,
Lodato L, Patrick M, Spampinato L (2005) Volcanic processes
during the 2002–2003 flank eruption at Stromboli volcano
detected through monitoring with a handheld thermal camera.
J Geophys Res
Crisp J, Baloga S (1990) A method for estimating eruption rates of
planetary lava flows. Icarus 85:512–515
Dehn J, Patrick MR, Harris AJL, Ripepe M, Calvari S (2004)
Handheld infrared imaging of strombolian eruptions. Bull
Volcanol: in review
Francalanci L, Tommasini S, Conticelli S, Davies GR (1999) Sr
isotope evidence for short magma residence time for the 20th
century activity at Stromboli volcano, Italy. Earth Plan Sci Lett
167:1–69
Harris AJL, Neri M (2002) Volumetric observations during paroxysmal
eruptions at Mount Etna: pressurized drainage of a shallow
chamber or pulsed supply? J Volcanol Geotherm Res 116:79–
95
Harris AJL, Stevenson DS (1997) Magma budgets and steady-state
activity of Vulcano and Stromboli volcanoes. Geophys Res Lett
24:1043–1046
Harris AJL, Butterworth AL, Carlton RW, Downey I, Miller P,
Navarro P, Rothery DA (1997) Low cost volcano surveillance
from space: case studies from Etna, Krafla, Cerro Negro, Fogo,
Lascar and Erebus. Bull Volcanol 59:49–64
Harris AJL, Flynn LP, Keszthelyi L, Mouginis-Mark PJ, Rowland
SK, Resing JA (1998) Calculation of Lava Effusion Rates from
Landsat TM Data. Bull Volcanol 60:52–71
Harris AJL, Murray JB, Aries SE, Davies MA, Flynn LP, Wooster
MJ, Wright R, Rothery DA (2000) Effusion rate trends at Etna
and Krafla and their implications for eruptive mechanisms. J
Volcanol Geotherm Res 102:237–269
Jeffreys H (1925) The flow of water in an inclined channel of
rectangular section. Phil Mag 49:793–807
Kauahikaua J,ManganM, Heliker C, Mattox T (1996) A quantitative
look at the demise of a basaltic vent: the death of Kupianaha,
Kilauea Volcano, Hawai’i. Bull Volcanol 57:641–648
Kneizys FX, Shettle EP, Gallery WO, Chetwynd JH, Abreu LW,
Selby JEA, Clough SA, Fenn RW (1983) Atmospheric transmittance/
radiance: computer code LOWTRAN 6. Air Force
Geophysics Laboratory, Environmental Research Paper 846,
Hanscom AFB, MA
Keszthelyi L, Denlinger R (1996) The initial cooling of pahoehoe
flow lobes. Bull Volcanol 58:5–28
Keszthelyi L, Harris AJL, Dehn J (2003) Observations of the effect
of wind on the cooling of active lava flows. J Geophys Res
30:SDE 4-1–SDE 4-4
Marchetti E, Ichahara M, Ripepe M (2004) Propagation of acoustic
waves in a viscoelastic two-phase system: influence of gas
bubble concentration. J Volcanol Geotherm Res: in press
Nappi G, Renzulli A (1989) Stromboli. Bull Volcanic Eruptions
26:1–3
Ripepe M, Gordeev E (1999) Gas bubble dynamics model for shallow
volcanic tremor at Stromboli. J Geophys Res 104:10639–10654
Patrick M (2002) Numerical modeling of lava flow cooling applied
to the 1997 Okmok eruption: comparison with AVHRR thermal
imagery. MSc thesis University of Alaska Fairbanks: 141 p
Pieri DC, Baloga SM (1986) Eruption rate, area, and length relationships
for some Hawaiian lava flows. J Volcanol Geotherm
Res 30:29–45
RossiM, SbranaA(1988) Stromboli. BullVolcanic Eruptions 25:7–8
Shaw HR (1969) Rheology of basalt in the melting range. J Petrol
10:510–35
Sutton AJ, Elias T, Kauahikaua J (2003) Lava-effusion rates for the
Pu’u ‘ ¨ O’¨o-K¨upaianaha eruption derived from SO2 emissions
and very low frequency (VLF) measurements. USGS Prof
paper 1676:137–148
Wright R, Blake S, Harris A, Rothery D (2001) A simple explanation
for the space-based calculation of lava eruptions rates. Earth
Planetary Sci Lett 192:223–233
Wooster MJ, Wright R, Blake S, Rothery DA (1997) Cooling mechanisms
and an approximate thermal budget for the 1991–1993
Mount Etna lava flow. Geophys Res Lett 24(24):3277–3280
Sulphur output and magma degassing budget of Stromboli
volcano. Nature 368:326–330
Calvari S, Neri M, Pinkerton H (2002) Effusion rate estimations
during the 1999 summit eruption on Mount Etna, and growth of
two distinct lava flow fields. J Volcanol Geotherm Res 119:107–
123
Calvari S, Andronico D, Burton MR, Dehn J, Garf`ı G, Harris A,
Lodato L, Patrick M, Spampinato L (2005) Volcanic processes
during the 2002–2003 flank eruption at Stromboli volcano
detected through monitoring with a handheld thermal camera.
J Geophys Res
Crisp J, Baloga S (1990) A method for estimating eruption rates of
planetary lava flows. Icarus 85:512–515
Dehn J, Patrick MR, Harris AJL, Ripepe M, Calvari S (2004)
Handheld infrared imaging of strombolian eruptions. Bull
Volcanol: in review
Francalanci L, Tommasini S, Conticelli S, Davies GR (1999) Sr
isotope evidence for short magma residence time for the 20th
century activity at Stromboli volcano, Italy. Earth Plan Sci Lett
167:1–69
Harris AJL, Neri M (2002) Volumetric observations during paroxysmal
eruptions at Mount Etna: pressurized drainage of a shallow
chamber or pulsed supply? J Volcanol Geotherm Res 116:79–
95
Harris AJL, Stevenson DS (1997) Magma budgets and steady-state
activity of Vulcano and Stromboli volcanoes. Geophys Res Lett
24:1043–1046
Harris AJL, Butterworth AL, Carlton RW, Downey I, Miller P,
Navarro P, Rothery DA (1997) Low cost volcano surveillance
from space: case studies from Etna, Krafla, Cerro Negro, Fogo,
Lascar and Erebus. Bull Volcanol 59:49–64
Harris AJL, Flynn LP, Keszthelyi L, Mouginis-Mark PJ, Rowland
SK, Resing JA (1998) Calculation of Lava Effusion Rates from
Landsat TM Data. Bull Volcanol 60:52–71
Harris AJL, Murray JB, Aries SE, Davies MA, Flynn LP, Wooster
MJ, Wright R, Rothery DA (2000) Effusion rate trends at Etna
and Krafla and their implications for eruptive mechanisms. J
Volcanol Geotherm Res 102:237–269
Jeffreys H (1925) The flow of water in an inclined channel of
rectangular section. Phil Mag 49:793–807
Kauahikaua J,ManganM, Heliker C, Mattox T (1996) A quantitative
look at the demise of a basaltic vent: the death of Kupianaha,
Kilauea Volcano, Hawai’i. Bull Volcanol 57:641–648
Kneizys FX, Shettle EP, Gallery WO, Chetwynd JH, Abreu LW,
Selby JEA, Clough SA, Fenn RW (1983) Atmospheric transmittance/
radiance: computer code LOWTRAN 6. Air Force
Geophysics Laboratory, Environmental Research Paper 846,
Hanscom AFB, MA
Keszthelyi L, Denlinger R (1996) The initial cooling of pahoehoe
flow lobes. Bull Volcanol 58:5–28
Keszthelyi L, Harris AJL, Dehn J (2003) Observations of the effect
of wind on the cooling of active lava flows. J Geophys Res
30:SDE 4-1–SDE 4-4
Marchetti E, Ichahara M, Ripepe M (2004) Propagation of acoustic
waves in a viscoelastic two-phase system: influence of gas
bubble concentration. J Volcanol Geotherm Res: in press
Nappi G, Renzulli A (1989) Stromboli. Bull Volcanic Eruptions
26:1–3
Ripepe M, Gordeev E (1999) Gas bubble dynamics model for shallow
volcanic tremor at Stromboli. J Geophys Res 104:10639–10654
Patrick M (2002) Numerical modeling of lava flow cooling applied
to the 1997 Okmok eruption: comparison with AVHRR thermal
imagery. MSc thesis University of Alaska Fairbanks: 141 p
Pieri DC, Baloga SM (1986) Eruption rate, area, and length relationships
for some Hawaiian lava flows. J Volcanol Geotherm
Res 30:29–45
RossiM, SbranaA(1988) Stromboli. BullVolcanic Eruptions 25:7–8
Shaw HR (1969) Rheology of basalt in the melting range. J Petrol
10:510–35
Sutton AJ, Elias T, Kauahikaua J (2003) Lava-effusion rates for the
Pu’u ‘ ¨ O’¨o-K¨upaianaha eruption derived from SO2 emissions
and very low frequency (VLF) measurements. USGS Prof
paper 1676:137–148
Wright R, Blake S, Harris A, Rothery D (2001) A simple explanation
for the space-based calculation of lava eruptions rates. Earth
Planetary Sci Lett 192:223–233
Wooster MJ, Wright R, Blake S, Rothery DA (1997) Cooling mechanisms
and an approximate thermal budget for the 1991–1993
Mount Etna lava flow. Geophys Res Lett 24(24):3277–3280
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