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Effects of magma compressibility
on volcano deformation and seismicity
Eleonora Rivalta
Outline
Interaction between magma-filled deformation sources:
1) Magma chamber ↔ dyking2) Magma chamber ↔ magma chamber3) Dyke ↔ faulting
and the role played by compressibility in the dynamics of these interactions.
1 -The 'missing magma' problem:the 1997 intrusion at Kilauea
(Owen et al., 2000)
= 3.8
Summit: -1.5 106 m3
Makahopuhi: -1.2 106 m3
Pu'u O'o: -12.7 106 m3
Dike: 23 106 m3
r V =V dyke
ΔV chamber
The 2007 'father's day' intrusion
(Montogomery-Brown et al., 2010, JGR)
rV = 3.0
Summit: -1.8 106 m3
Pu'u O'o: -0.02 106 m3
Dike 1: 0.8 106 m3
Dike 2: 15.8 106 m3
Pu'u O'o lake: -3.65 106 m3
The 2007 intrusion at Kilauea
(Montogomery-Brown et al., 2011)
The 'missing magma' problem:the 2005 intrusion in Afar
Wright et al., 2006
The 'missing magma' problem:the 2005 intrusion in Afar
Wright et al., 2006
r V =V dyke
ΔV chamber∼
∼ 2.5 km3
(0.25+0.25)km3=5
Interpretation
An additional source, too deep to be detected from deformation signals, fed the intrusion from below. → In general, difficult to test/falsify
Volume determinations are not reliable→ Not to the extent required to explain these discrepancies
Magma compressibility
Different source compliance
Effects of magma compressibilityon volcano deformation
Árnadóttir et al., 1998
Johnson et al., 2000
Johnson, 1992
Mastin et al., 2008
Magma compressibility and elastic responseof host rock mask the 'true volume' of the intrusionAppl. to volume budget of 1984 intrusion at Krafla
Tryggvason, 1981 Pressure variation and volume change at theKrafla magma reservoir
Considerations on the different volumes involved
Application to the relation between eruptedand deflation volumes at Mount St. Helens
Rivalta and Segall, 2008 'Mass conservation', volume budget during intrusion events
Rivalta, 2010 Dynamics of coupling between magma chambers and dikes
Physical model
dM=ρdV+V d ρ=(ρ dVdp
+Vd ρdp
)dp=ρV (βe+βm)dp
βe(spherical chamber )=3
4μ∼10−11−10−10Pa−1
βe(penny shaped crack )=1
pi−σ∼10−7Pa−1
(or much higher if magma contains bubbles)
βm=10−11−10−10Pa−1
Magma compressibility: Source compliance:
βm=1ρd ρdp
βe=1VdVdp
Physical model
If total mass is constant →
dM=ρdV+V d ρ=(ρ dVdp
+Vd ρdp
)dp=ρV (βe+βm)dp
r V=V i
ΔV c=1+βmβe
βe(spherical chamber )=3
4μ∼10−11−10−10Pa−1
βe(cigar−shaped chamber )=1μ
βe(ellipsoid ) depends on the aspect ratio
βe(penny shaped crack )=1
pi−σ∼10−7Pa−1(or much higher
if magma contains bubbles)
βm=10−11−10−10Pa−1
(Amoruso and Crescentini, 2009)
Rivalta and Segall, 2008
Physical model
Rivalta and Segall, 2008
The 'missing magma' problem:chronology
5 – 6 (Árnadóttir et al., 1998)1984 Krafla (Iceland)
1997 Kilauea (Hawaii) 3.8 (Owen et al., 2000)
2007 Kilauea (Hawaii) 3.0 (Montgomery-Brown et al., 2011)
2000 Miyakejima (Japan) 3.6 (Irwan et al., 2006)
2005 Manda-Harraro (Ethiopia) 5 - 2.2Grandin et al., 2009)
2007 Ferdinandina (Galapagos)
2004 Dallol (Ethiopia)
Year location rV
Ref
32 (Nobile et al., 2012, subm.)
2.6(Bagnardi and Amelung, 2012, subm.)2009 Ferdinandina (Galapagos) 2.0
(Wright et al., 2006,
Wright et al., 2012
The 2005 dike intrusion in Afar
Ayele et al., 2009
The 2005 dike intrusion in Afar
- 0.12 km3
ΔV Chambers:
ΔV Dike: +1.5 km^3
- 0.12 km3ΔV Chambers:
ΔV Dike: +2.0 km3
r_V = 2.2
ΔV Dike / ΔV Chambers =r_V = 2.8
- 0.42 km3
- 0.42 km3
- 0.37 km3
Grandin et al., 2009
Fernandina, Galapagos
rV = 2.6
Fernandina, Galapagos
rV = 2.0
Dallol, Ethiopia, 2004
(Nobile et al., 2011)
Dallol, Ethiopia
The 1997 intrusion at Kilauea
(Owen et al., 2000)
The 'missing magma' problem in volcano deformation
Einarsson and Brandsdottir, 1978
~ 2 km/h
~ 0.3 km/h
Izu Islands (Japan), 2000
Irwan et al., 2006
Physical model
dM i
dt=k pc−p i
dM c
dt=−k pc−p i dM
dt=ρV (βe+βm)dp
dt
On the other hand:On one hand:
k=ρmπR4
8ηLFor a cylindrical conduitL long and with radius R: (Pinel and Jaupart, 2003)
dp idt
=−p i−pc
, =
8L mV i em
mR4sphere=
8L r 314 m
3
R4
p.s.c.=641− La3
3R4
~ weeks to months
dM
Physical modeldp idt
= − 1i
p i−pc
dpcdt
= 1c
p i−pc
∫p1c
pc
dMOutc ∫
p i
dM i=0
Rivalta, 2010
The flow will stop when pc=pi=peq
V c=V 1c c p1
c−peqe− t
W=−V 1cc
W1W
pE 1−e− t
W
V i= b1W
pE 1−e− t
W
Chamber's volume loss:
Dike's volume:r V=
V i
V c=1mc
at any time!W=dike
sphere= bV 1c mc
i1W
=W c1W
≡W
Physical model
Rivalta, 2010
● Different timescales for dischargeand recharge
r V=V i
V c=1mc
at any time!
● Convexity upwards
● Strong dependence on βm, β
c
Validation: 2000 intrusion at Izu Islands
Rivalta, 2010
Validation: 2000 intrusion at Izu Islands
Rivalta, 2010
Pattern of induced seismicity
Keir et al., 2009
Belachew et al., 2011
'Vertical' dike propagation
(Bonforte et al., 2008, JGR)(Battaglia et al., 2011, JVGR)
Vertical propagation and stacked sills
(Sigmundsson et al., 2010)
Harrat Lunayyir, Saudi Arabia, 2009
(Pallister et al., 2011, Nature Geoscience)
2 - Interacting magma chambers
Interacting magma chambers
(Pascal et al., 2012, submitted)
Interacting magma chambers
Perspectives:
● Varying shapes ● Interacting sources (e.g. boundary elements)● Include magma properties (compressibility)● Dynamics of filling/emptying
3 - Magma compressibilityand dyke-faulting interaction
Magma compressibilityand dyke-faulting interaction
Δσ → ux
i
Δσ+ΔσF → ux
i + ∆ux
i
→ ∆V
Magma compressibilityand dyke-faulting interaction
MT fault=μ Af (0000
sin2 θ−cos2 θ
0− cos2 θ−sin2 θ )
MT Δdike=Ad ( λΔuμΔu j
0
μΔu j
(λ+2μ)ΔuμΔuk
μΔu k
0λΔu )
Magma compressibilityand dyke-faulting interaction
Magma compressibilityand dyke-faulting interaction
Induced earthquakes interact with dykes, which respond with a shearing and change of opening.
● Apparent rotation of the fault planes (up to ~27 degrees)● For low gas content & mass constant, pure DC● For higher gas content, significant isotropic and CLVD component● CLVD is physical: contraction/inflation of the dyke during the
earthquake
Perspectives
● Effects of compressibility are multifaceted and not intuitive● It helps thinking about 'mass' rather than volume● How much of the recurrent volume-multiplications observed
during dyking is due to magma compressibility and source compliance?
● More statistics will help us find/understand patterns: sill/dyke, magma composition, volatile content, depth of sources, geometry? → insight into plumbing at depth
● Dynamics of the plumbing● We need to understand more the influence of gas (bubble
nucleation, exsolution, type of degassing) on the observables (deformation, seismicity)
Acknowledgements
● Paul Segall● Maurizio Bonafede● Torsten Dahm● Emily Montgomery-Brown● Larry Mastin● Tim Wright● Derek Keir● Karen Pascal● Carolina Pagli● Adriano Nobile
● Francesco Maccaferri● Luigi Passarelli● Yosuke Aoki● Marco Bagnardi● Valerio Acocella