RESEARCH Open Access
The 1831 eruption of Babuyan Claro thatnever happened: has the source of one ofthe largest volcanic climate forcing eventsof the nineteenth century beenmisattributed?Christopher S. Garrison* , Christopher R. J. Kilburn and Stephen J. Edwards
Abstract
The 1831 eruption of Babuyan Claro in the Philippines is regarded as one of the most significant volcanic climateforcing events of the nineteenth century. Modern databases have assigned the eruption a VEI of 4? and Magnitudeof 4.7. Our analysis of historical sources, however, suggests that there was no such eruption in 1831 and that thisdate is the result of a misinterpretation of a traveller’s account which had been taken to be the primary source. Wetherefore suggest that the 1831 eruption is a false event. In this case, one or more eruptions elsewhere must havebeen responsible for producing the climate-impacting stratospheric sulphate aerosol in 1831. Our results reveal theneed to re-evaluate the hazard assessment of Babuyan Claro volcano and also, potentially, the quantitative treatmentof the 1831 stratospheric sulphate aerosol in climate models. The Babuyan Claro example discussed in this papertherefore reinforces a call for the careful analysis of primary historical sources in volcanology.
Keywords: False eruption, Misattributed eruption, Historical, Volcanology, Climatology
IntroductionVolcanic eruptions that produce sulphate aerosols inthe stratosphere are important climate forcing events(Robock 2000). A body of evidence points to such aneruption in 1831. Unusual atmospheric optical phenomenawere observed around the world in August, September andOctober 1831, including a high haze, a dimmed blue orgreen sun and ‘volcanic’ sunsets (Arago 1832; Kiessling1888; Symons 1888). When the Krakatoa Committee ofthe Royal Society of London was searching for analo-gous examples of the optical phenomena seen after the1883 eruption of Krakatoa, in Indonesia, they identifiedthose in 1831, along with those observed in 1783 afterthe Grímsvötn (Laki) eruption, in Iceland, as the twomost similar to have been reported in the previous fourcenturies (Symons 1888). Anomalous surface temperatures(regionally warmer or cooler than normal) occurred
between 1831 and 1833 (White et al. 1997; Shindell et al.2004; Fischer et al. 2007; McCarroll et al. 2013). Asulphate peak detected in ice-cores from Greenland whichis ranked as either the second (Zielinski et al. 1994), third(Sigl et al. 2013) or fifth (Gao et al. 2008) largest of thenineteenth century has been dated to 1831, with depos-ition continuing until 1833 (Sigl et al. 2013). Even ifranked fifth (Gao et al. 2008), the only larger nineteenthcentury peaks are those produced by the eruptions ofTambora (1815, Indonesia), Unknown (1809), Cosegüina(1835, Nicaragua) and Krakatoa.The largest magnitude eruption listed for 1831 in the
standard catalogue of historical volcanism (the Smithson-ian Global Volcanism Program (GVP) database) is that ofBabuyan Claro, in the Philippines, with a Volcanic Explo-sivity Index (VEI) of ‘4?’ (GVP 2013). The question markindicates a VEI value that was “particularly difficult to as-sign [or was] based on purely circumstantial evidence”(Simkin et al. 1981). A VEI ≥ 4 is associated with a ‘defin-ite’ stratospheric injection of eruption products (Newhall
* Correspondence: [email protected] Hazard Centre, Department of Earth Sciences, University CollegeLondon, Gower Street, London WC1E 6BT, UK
© The Author(s). 2018 Open Access This article is distributed under the terms of the Creative Commons Attribution 4.0International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, andreproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link tothe Creative Commons license, and indicate if changes were made.
Garrison et al. Journal of Applied Volcanology (2018) 7:8 https://doi.org/10.1186/s13617-018-0078-9
and Self 1982). This eruption has therefore commonlybeen inferred to be the likely source of the 1831 strato-spheric sulphate aerosol (Zielinski et al. 1994; White et al.1997; Fischer et al. 2007; Sigl et al. 2013) and, given themagnitude of the associated Greenland sulphate peak, it isregarded as one of the most significant volcanic climateforcing events of the nineteenth century, particularly sowhen treated as a double eruption with the 1835 (VEI = 5)eruption of Cosegüina, producing ‘enhanced’ forcing ef-fects over a decadal time frame (Zielinski 1995; Arfeuilleet al. 2014; Longpré et al. 2014; Toohey & Sigl 2017). Thiseruption is also listed in the Large Magnitude ExplosiveVolcanic Eruptions (‘LaMEVE’) database (the thresholdfor inclusion in which is a VEI of at least 4), with a Magni-tude (M) of 4.7 (Crosweller et al. 2012).However, the record of the 1831 eruption of Babu-
yan Claro in the GVP database is based solely on his-torical observations (GVP 2013) and Zielinski (1995)has highlighted the need for the ‘thorough study’ of this‘less well known’ eruption. In this paper we identify andanalyse the relevant historical observations to investigateif they are commensurate with the suggested VEI andMagnitude (Crosweller et al. 2012; GVP 2013). Our ana-lysis shows that, to the contrary, there is no reason to be-lieve that Babuyan Claro did erupt in 1831 and that itsrecord in the present-day literature is the result of mis-taken assumptions. We therefore suggest that the 1831eruption of Babuyan Claro is a false event and that oneor more alternative eruptions will have to be identifiedas the source of the 1831 stratospheric sulphate aerosol.
MethodHistorical sources (typically written records) can generallybe divided into two categories. ‘Primary’ sources providefirst-hand evidence of a historical event, for example con-temporaneous eye-witness statements. ‘Secondary’ sourceslater mention, discuss or interpret those primary sources.Primary sources are therefore of paramount importance inproviding the evidentiary base for the secondary sources.Since the primary sources for the 1831 eruption of Babu-yan Claro were not immediately identified in the GVPdatabase (GVP 2013), we identified them according to thefollowing method.An initial set of sources was selected from the refer-
ences and bibliographies of the successive editions of theVolcanoes of the World (Simkin et al. 1981; Simkin andSiebert 1994; Siebert et al. 2010; GVP 2013). The earliersources from which they drew their information werethen identified by the multi-step process illustrated inFig. 1. In some cases, an earlier source could be identi-fied explicitly where cited with a complete reference.In other cases its identity could be inferred, for example,on the basis of a partial reference. The multi-step processwas repeated iteratively for successively earlier sources,
tracing several routes back through the literature, until theprimary source(s) for the eruption had been obtained.A total of 39 sources were analysed for the 1831 eruption
of Babuyan Claro (written in English, French, German andItalian), as well as two supplementary sources from before1831 that mention Babuyan Claro island (written inEnglish and Spanish). These included the standard cata-logues of historical volcanism by von Hoff (1841), Daubeny(1848), Landgrebe (1855), Scrope (1862), Fuchs (1865),von Humboldt (1869), Mercalli (1907), Schneider (1911),Sapper (1917, 1927), Catalogue of the Active Volcanoes ofthe World (CAVW) (1951–1975) [Part II: PhilippineIslands and Cochin China (van Padang 1953)] andMacdonald (1972). Table 1 contains an entry for eachsource including (i) textual extracts along with translationsinto English where necessary; (ii) a classification as to pri-mary (‘P’) or secondary (‘S’) source type where appropriate;and (iii) in the case of secondary sources, a list of the earl-ier sources (if any could be identified) on which they werebased.
Results and discussionThe single primary source for the 1831 eruption ofBabuyan ClaroFigure 2 shows the network of routes traced back throughthe sources for the 1831 eruption of Babuyan Claro. Astriking feature is that they all lead to Meyen (1835) as theprimary source.In 1835, Franz Julius Ferdinand Meyen (b. 1804, d.
1840) published ‘Reise Um Die Erde’ (Voyage Round theWorld), an account of his round-the-world voyage (1830–1832) aboard the Prinzess Louise (Meyen 1835; CDSB2008). He had previously trained as a surgeon and publishedan important work in the field of botany (Meyen 1830;CDSB 2008).In July 1831 the Prinzess Louise left the Hawaiian islands
for China. The ship passed the remote island of BabuyanClaro whilst traversing the channel between the Philippinesand Taiwan (Fig. 3). The island forms a part of the Luzonvolcanic arc (Defant et al. 1990) and has two active vol-canoes: the stratovolcano Babuyan Claro, which rises to1080 m. a.s.l. at the centre of the island, and Smith vol-cano, a smaller cone at the western end of the islandwith a peak at 688 m. a.s.l. (GVP 2013) (Fig. 4).On page 181 of volume 2 of his account, Meyen records
that: “…We chose to approach through the BalingtangStraits and, on the following morning [7th August 1831],had the Island of Babuyan in view on the left and theIsland of Balingtang on the right. The mountains ofBabuyan could exceed a few thousand feet in height,their western peak forming a steep cone, which is prob-ably the volcano which only a short time ago hadcaused the inhabitants of the Island to flee. Balingtang
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 2 of 21
island has some strangely shaped rocks in its vicinity…”(Meyen 1835, italics added; Table 1).The western peak is Smith volcano. The italicised sen-
tence is Meyen’s only reference to a volcano on BabuyanClaro island in his whole account. Assuming a straightline between the ship positions that Meyen noted in hismeteorological log for 12 h on the 6th August and 18 hon the 7th August (Meyen 1835), Fig. 3 shows the re-con-structed course of the Prinzess Louise. The reconstructionsuggests that Meyen would still have been about 14 kmdistant at his closest approach.Meyen evidently believed (a) that a volcanic event had
taken place on the island, ‘probably’ at Smith volcano; (b)that it had caused the inhabitants of the island to flee; and(c) that it had occurred ‘only a short time ago’. However,his use of the term ‘probably’ indicates that he couldnot have observed any unambiguous evidence of a recenteruption. Prior to his passage past the island, his accountcontains no record of any of the phenomena, such ascannon-like booms, smoke columns or ash fall, whichmight have evidenced an eruption nearby (although, co-incidentally, it appears that he did observe at least oneof the unusual atmospheric optical phenomena which
were being seen around the world at the same time, seeMeyen 1835; Table 1). His account includes no recordof having met any of the fleeing inhabitants or, indeed,of having met anyone else who had done so. His use ofthe phrase ‘only a short time ago’ is difficult to interpretbecause elsewhere in his account he uses similar phrasesto indicate intervals from hours to decades, depending onthe context (Meyen 1835). Meyen’s (1835) account there-fore provides no suggestion that he was reporting a vol-canic event which he had witnessed himself. Rather, it ismore likely that he was reporting one which he had readabout (or otherwise become aware of) from an unacknow-ledged source describing an earlier event which had driventhe inhabitants of the island to flee.We have identified evidence pointing to at least one
such event. The eighteenth century historian Vicente deSalazar reported that, in 1681, a volcano on top of a highmountain on Babuyan Claro island threw out ‘fire, rocksand ash’ and produced a ‘huge boom’ (de Salazar 1742;Table 1). Although this description points to a compara-tively modest eruption, de Salazar (1742; Table 1) furtherreported that Fr. Matheo Gonçalez, a Dominican priestvisiting the island at the time, drew a vivid comparison
Fig. 1 Flowchart illustrating the method used to identify the primary source(s)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 3 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
1GlobalV
olcanism
Prog
ram
(2013)
[Volcano
esof
theWorld,4th
ed.]
“Startdate:1831,Stop
date:U
nkno
wn,Erup
tionCertainty:
Con
firmed
,VEI:4?,Eviden
ce:H
istoricalObservatio
ns,
Activity
Areaor
Unit:Babu
yanClaro”(‘H
olocen
eSpreadsheet’do
wnloadablefro
mtheGVP
database)
N.BWhe
nview
ingtheerup
tivehistoryof
Babu
yanClaro
volcanothroug
hthe‘Volcano
Search’optionof
theGVP
database,a
VEI=
4(with
outthequ
estio
nmarkmod
ifier)
ispresen
ted.How
ever
thisisseem
inglyan
artefact
oftheweb
interface
andtheVEI=
4?presen
tedin
the
authoritativeHolocen
espreadsheetdata
downloadable
from
theGVP
database
isthecorrectvalue(pers.comm.
Dr.BenAnd
rews,Sm
ithsonian
Institu
tion,28/04/2016).
S‘Referen
ces’un
der‘Gen
eral
Inform
ation’
2Sieb
ertet
al.(2010)
[Volcano
esof
theWorld,3rd
ed.]
“Start:1831,Duration:?,Vo
lcanoNam
e:Babu
yanClaro
(Luzon
-Nof),Num
ber:0704–03=
,VEI:4?,Vo
lV/T:−
/8”
(p.260)
SStandard
catalogu
esof
historical
volcanism
(p.1),‘Referen
ces’
(pp.479et
seq.)
3PH
IVOLC
S(2008)
“Nam
e:Babu
yanClaro,Year:1831,Site:C
rater,Erup
tion
Character:Explosive.”
SVanPadang
(1953)
4SimkinandSieb
ert(1994)
[Volcano
esof
theWorld,2nd
ed.]
“Start:1831,Duration:?,Vo
lcanoNam
e:Babu
yanClaro
(Luzon
-Nof),Num
ber:0704–03=
,VEI:4?,Vo
lV/T:−
/8”
(p.207)
SStandard
catalogu
esof
historical
volcanism
(p.1),‘Referen
ces’
(pp.303et
seq.)
5Simkinet
al.(1981)
[Volcano
esof
theWorld,1sted
.]“Volcano
Nam
e:BA
BUYA
NCLA
RO(LUZO
NIS-N
OF),
Num
ber:0704–03”
(p.64)
“Volcano
Nam
e:SM
ITHVO
LCANO(LUZO
NIS-N
OF),
Num
ber:0704–04=
,STA
RT:1831,ERUPTIVE
CHARA
CTERISTICS[Three
symbo
ls:C
entralcrater
erup
tion,no
rmalexplosions,d
estructio
nof
land
,prop
erty],VEI:3?,VVLT:−
8[norecorded
lava
volume,0.1km
3teph
ra”(p.64)
SStandard
catalogu
esof
historical
volcanism
(p.1),‘Bibliography’
(pp.215et
seq.)
6COMVO
L(1981)
“Nam
e:Babu
yanClaro…Its
firsterup
tionwas
repo
rted
in1831.”
SVario
uslate
C19
thandC20
th
sourcesinclud
ingVanPadang
(1953),Saderra
Masó(1924),
Smith
(1924),Saderra
Masó(1904).
7MacDon
ald(1972)
N.B.N
oreferenceto
an1831
erup
tionof
Babu
yanClaro.
n/a
n/a
8Lamb(1970)
“vii-viii.1831...Babuyan
(Babujan),Ph
ilipp
ineIs.
(H,K,S,Sh)...19oN122°E…
(Sappe
r’sassessmen
t)b 2…d.v.i./E m
ax=300.”(p.514)
“...The
Babu
yanerup
tionisge
nerally
accepted
asagreat
one.”(p.515)
SHum
phreys
(1940)
Shaw
(1936)
Sapp
er(1917,1927)
Symon
s(1888)
9VanPadang
(1953)
[CAVW
,PartII:Ph
ilipp
ineIsland
sandCochinChina]
“I.Nam
eandlocatio
n...BABU
YANCLA
RO(7,4–3).”
(p.42)
“I.Nam
eandlocatio
n...SMITHVO
LCANO(7,4–4)…
III.
Volcanicactivity.Som
eof
theolde
rerup
tions
may
have
been
ofBabu
yanClaro
(7,4–3)…
1831
[Three
symbo
ls:
Erup
tionin
thecentralcrater,no
rmalexplosions,
destructionof
arableland
].”(p.43)
SBecker
(1901)
Smith
(1924)
Sade
rraMasó(1905,1924,1925)
Alvir(1928)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 4 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
10Hum
phreys
(1940)
“Atanyrate,volcanicdu
stisso
fine,andtheup
per
atmosph
ereabove11
kmso
freefro
mmoistureand
verticalconvectio
n,that
once
such
dustisthrown
into
thisregion
,asitob
viou
slywas
bytheexplosions
ofSkaptarJökull,andAsamayam
a,in
1783;Babuyan,in
1831...itmustrequ
ire,asarule,b
ecause
ofits
slow
descen
t,fro
m1to
3yearsto
getback
totheearth.”
(pp.
593–594)
“Date:1831–1832…
Natureof
Discrep
ancy:C
old…
Prob
able
Cause:…
Babu
janIsland
s,1831”(p.615)
S–
11Shaw
(1936)
“Volcanicerup
tions
sinceA.D.1800…
1831
Babu
yanClaro.”
(v.2,p
.25)
S–
12Alvir(1928)
“Babuyan
Claro
-Thisvolcanowas
repo
rted
tohave
erup
tedin
1919.”(p.758)
n/a
n/a
13Sapp
er(1927)
“Zum
philipp
inischen
System
(1)ge
hörenfolgen
deVu
lkanzone
n:[...]
5.Babu
yanClaro,1000m,in19o40’N
.Br.,121o
56′
Ö.L.,hatte1831
heftigen
A.,de
ssen
Feinaschen
inEuropa
Däm
merun
gsersche
inun
genverursacht
habe
ndü
rften
(neuerding
sbe
zweifelt).Tätig
um1860.1917un
d1918
Anzeichen
neuerTätig
keit.
[...]
(1)Neuenachrichten
inM.Saderra
Masó,Active
Philipp
ineVo
lcanoe
s(Bull.Weather
Bureau
April
1922)Manila,A
uszugin
Bull.volcanolog
ique
1925,S.306–310.”(p.320)
[Translatio
n:“The
followingvolcaniczone
sbe
long
tothePh
ilipp
inesystem
(1):
[...]
“5.Babuyan
Claro,1000m,...un
derw
entapo
werful
erup
tionin
1831,w
hose
fineashe
scouldhave
caused
thetw
iligh
teffectsin
Europe
(recently
questio
ned).
[...]
(1)New
inform
ationin
M.Saderra
Masó,Active
Philipp
ineVo
lcanoe
s(Bull.Weather
Bureau
April1922)
Manila,Sum
maryin
Bull.volcanolog
ique
1925,S.306–310.”]
N.B.Itisinterestingthat
Sapp
erintrod
uces
theph
rase
‘recentlyqu
estio
ned’
tohis1927
entryforthiserup
tion.
Heciteson
lySade
rraMasó(1922),the
summaryof
which
presen
tedin
Sade
rraMasó(1925)
states
that
apreciseknow
ledg
eof
thedatesof
historicalerup
tions
ofBabu
yanClaro
volcanois‘rather
wantin
g’.H
owever,
even
ifSapp
erdiden
tertainanysuch
doub
tsin
1927,
thereisno
eviden
ceto
sugg
estthat
they
constraine
dtheuseof
his1917
teph
ravolumerang
eby
laterauthors.
SSade
rraMasó(1922,1925)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 5 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
14Sade
rraMasó(1925)
“Claro
Babu
yanVo
lcano.Ontheisland
ofBabu
yanne
arthecenter
at19
o40’N
,121
o56
E.Since1656,w
hen
Dom
inican
Mission
ariesvisitedtheisland
forthefirst
time,ithasbe
enrepo
rted
asactivebu
tprecisedates
oferup
tions
arerather
wantin
g.In
1907
WORC
ESTER
took
photog
raph
swhich
show
twone
wrecent
craters.
In1917,W
.D.SMITHof
theBu
reau
ofMines,visitedit
andfoun
dconvincing
indicatio
nsof
recent
outbursts.
Morerecently,M
ay17th
and19th,1918,Captain
ROSÉS
oftheinterisland
S.S.“M
auban”
onsailing
closeto
the
island
saw
thevolcanoin
erup
tion.Westof
themain
volcanorises
anothe
rremarkablewellp
reserved
cone
calledSm
ithvolcano,which
was
activewith
inthe
pastsixmon
ths.Severalo
fthevolcanoe
sappe
aring
inprevious
lists,asforinstances,thosepu
blishe
dby
PERRY,MARC
ALLIand
othe
rs,are
extin
ctvery
old
volcanoe
sof
theworn-do
wn-stocktype
;...”(pp.
385–386)
n/a
Mercalli(1907)
Perrey
(1860)
15Sade
rraMasó(1924)
(see
Sade
rraMasó1925)
16Sm
ith(1924)
“Ontheway,Iwas
enabledto
remainabou
ttw
oho
urs
onBabu
yanClaro,w
here
thereisavolcanowhich
has
been
activeas
recentlyas
1860.The
rearetw
ovolcanoe
son
thisisland
,one
abe
autifullysymmetricalcind
ercone
,abou
t2220
ft[670
m]inhe
ight,and
theothe
rless
symmetricalbu
tshow
ingtw
ocraterswhich
contain
steam
vents.Thesm
allervolcanocontains,b
esides
the
fineashthat
givesitits
shape,arecent
flow
ofscoriaceou
sbasalt.Theolde
rflowsof
thisvolcanoare
also
basaltic.Therehasbe
enno
serio
userup
tionsince
1860.The
few
peop
lelivingon
theisland
repo
rt,
however,thatsteam
explosions
occurred
onthesm
aller
mou
ntaintenyearsagoandon
thelarger
four
years
ago.Noashe
sreache
dthevillage
inanyof
these
explosions,how
ever.A
sitison
lyin
thelastthirty-five
yearsthat
theisland
hasbe
eninhabited,
the
inhabitantsknow
nothingof
theerup
tions
of1860.”
(p.264)
“BABU
YANCLA
RO.Fergu
sonsays:Babuyan
Island
isabou
t13
kmin
ano
rthe
astandsouthw
est
directionandhasan
averagewidth
ofabou
t10
km.
Atthewestern
pointisavolcano670m
high
.This
mou
ntainisconicalinshapeandeviden
tlycontains
asm
allcraterat
itssummit.Flow
sof
roug
hscoriaceou
sbasaltsurrou
ndthebase
andthe
mou
ntainitselfisbu
iltup
ofalternatingbasaltflows
andde
positsfro
mexplosiveerup
tions,ang
ular
basalt
fragm
ents,b
omblapilliandsm
allslaglikemasses.
Thewriter
hadan
oppo
rtun
ityto
land
here
fora
SBecker
(1901)
Fuchs(1881)
[Meyen
(1835)]
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 6 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
shorttim
eand,
althou
ghun
ableto
reachthesummit,
collected
specim
ensof
thebasaltfro
mon
eof
the
earlier
flowsandfro
mthelatestflow.Intheeastern
partof
theisland
isanothe
rvolcano,1160
min
height
andhe
avily
timbe
red.
Onits
southe
rnside
wereactivefumaroles.Severalerup
tions
ofthe
volcanoe
sof
thisisland
have
been
noted.
Horsburgh
in1817
men
tions
avolcanoon
the
western
point,thou
ghhe
does
speakof
any
erup
tionhaving
occurred
.Fuchs
[1881]
men
tions
anerup
tionas
having
occurred
in1831.Becker
quotes
Meyen
asmen
tioning
thiserup
tion,and
Sempe
ras
statingthat
Babu
yanClaro
seem
edthen
(1860)
tobe
continually
inerup
tion.”(p.304)
N.B.Itisinterestingthat,con
sisten
twith
Maree
(2005),Smith
becameaw
areon
hisbriefvisitto
Babu
yanClaro
island
that
ithadbe
enun
inhabited
tillcom
parativelyrecently(alth
ough
heseem
sto
have
been
unaw
arethat
ithadbe
enpreviously
inhabitedin
themoredistantpast).
17Sade
rraMasó(1922)
(see
Sade
rraMasó1925)
18Sapp
er(1917)
“Babuyan
Claro,1000m,hatte
1831
(5)eine
nhe
ftige
nAusbruch,de
ssen
Feinaschen
noch
inEuropa
schö
neDäm
merun
gsersche
inun
gen
mitverursachthabe
ndü
rften
(6).
[...]
(5)Masóa)
S.12.M
eyen
,Reise
II,S.181.
(6)Repo
rtof
theKrakatoa
Com
mittee
oftheRo
yal
Society.Lond
on1888.S.396.”(p.149)
[Translatio
n:“Babuyan
Claro,1000m,und
erwen
ta
powerfuleruptionin
1831
(5)thefineashe
sof
which
couldhave
contrib
uted
tothebe
autiful
twiligh
teffectseven
inEurope
(6).
[.] (5)Masóa)
P.12.M
eyen
,Reise
II,P.181.
(6)Repo
rtof
theKrakatoa
Com
mittee
oftheRo
yal
Society.Lond
on1888.P.396.”]
N.B.A
nearlier
reference(p.148)m
akes
clearthat
thefirstreferenceisto
Sade
rraMasó(1904).
“Tabellede
rbe
kann
tenRiesen
ausbrüche…
1831
Babu
yanClaro
b 2“(p
p.338–340)
[Translatio
n:“Tableof
know
nlarge
erup
tions…1831
Babu
yanClaro
b 2”]
“a1a 2
bede
utet
darin
wiede
rFörderun
gvonüb
er1bzw.1/10cbkm
Lava,b
1b 2
voneb
ensoviel
Lockermassen.“(p
.337)
[Translatio
n:“In
thefollowinga 1
a 2againde
notes
SSade
rraMasó(1904)
Symon
s(1888)
Meyen
(1835)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 7 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
theprod
uctio
nof
over
1or
1/10
km3of
lava,
b 1b 2
ofthesameam
ount
ofteph
ra.“]
19Schn
eide
r(1911)
“90...Babuyan
Claro...121
o56’3.19o30’n...A
usbrüche
:1831,1860.”(p.242)
[Translatio
n:“90...Babuyan
Claro...Eruptions:
1831,1860”]
S–
20Mercalli(1907)
“Babuyane-Claro
(1000m.),situatone
lleisole
Babu
yane
,che
form
anolapartepiù
setten
trionalede
ll’archipelago:eb
beun
’eruzion
emolto
fortene
l1831.”(p.305)
[Translatio
n:“Babuyane-Claro
(1000m.),
locatedin
theBabu
yanisland
s,which
form
the
northe
rnmostpartof
thearchipelago:un
derw
ent
apo
werfuleruptionin
1831.”]
SPerrey
(1860)
21Sade
rraMasó(1905)
“[Nam
e]Babu
yánClaro...[Dateof
erup
tion]
1831,
1860”(p.187)
S–
22Sade
rraMasó(1904)
“Nam
e:Babu
yánClaro...D
ateof
erup
tion:1831,
1860”(p.12)
S–
23Becker
(1901)
“The
remaining
volcanicmou
ntains
ofthe
archipelagolie
inon
egrou
pat
itsno
rthe
rnen
d.Mr.James
Horsburgh
men
tions
the
little
island
Cam
aguínde
Babu
yane
sas
having
form
erlybe
enavolcano,andsays
that
onthewesten
dof
theIsland
ofBabu
yan
Claro
thereisavolcano[re
f:Horsburgh
1817,
p.328].M
eyen
states
that
in1831
thelatter
unde
rwen
taviolen
terup
tion.Sempe
r[see
Sempe
r(1869)]saysBabu
yanClaro
seem
sto
becontinually
inerup
tion...”(p.54)
SSempe
r(1869)
Meyen
(1835)
Horsburgh
(1817)
24Symon
s(ed.)(1888)
[Rep
ortof
the
Krakatoa
Com
mittee
oftheRo
yal
Society]
“Babujan
Island
s,1831,(Great
erup
tion)”(p.396)
SJudd
(1881)
Daube
ny(1848)
25Fuchs(1884)
“Onconn
aîtplusieursvolcansdans
lespe
tites
îles
Bajuban,qu
ison
tsituéesau
nord
del’archipe
l.L’un
d’en
treeux,leClaro
Babyan
(10o
27′lat.Bor.
et110
o42′lon
git.or.),est.toujou
rsactif
eteut
uneérup
tionen
1831.”(p.236)
[Translatio
n:“Severalvolcanoe
sareknow
nin
theBajubanisles,which
arelocatedin
theno
rth
ofthearchipelago.One
ofthem
,Claro
Babyan...
isstillactiveandun
derw
entan
erup
tionin
1831.”]
S–
26Fuchs(1881)
(see
Fuchs1865,1884)
27Judd
(1881)
N.B.N
oreferenceto
an1831
erup
tionof
Babu
yanClaro.
n/a
n/a
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 8 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
28Vo
nHum
boldt(1869)
(see
vonHum
boldt1858)
29Sempe
r(1869)
N.B.N
oreferenceto
an1831
erup
tionof
Babu
yan
Claro
althou
ghSempe
rmen
tions
“…einwiees
sche
intin
beständige
rErup
tionbe
findliche
Vulcan
aufB
abuyan
Claro…
“(p.
14)
[Translatio
n:“…
avolcanoon
Babu
yanClaro
which
seem
sto
bein
constant
erup
tion…
”]
n/a
–
30Fuchs(1865)
“Zwischen
Form
osaun
dde
nPh
ilipp
inen
liege
nzw
eivulkanischeInseln,C
laro
Babyan
und
Cam
ingu
in.D
erVu
lkan
aufC
laro
Babyan
liegt
19o27′n
.Br.,119
o42′ö
stl.L.un
dhatnach
Meyen
1831
eine
nAusbruchge
habt.”(p.47)
[Translatio
n:“BetweenForm
osaandthePh
ilipp
ines
lietw
ovolcanicisland
s,Claro
Babyan
andCam
ingu
in.
Thevolcanoon
Babu
yanClaro...,accordingto
Meyen
,un
derw
entan
erup
tionin
1831.”]
SMeyen
(1835)
31Scrope
(1862)
“Som
eof
thelesser
island
swhich
conn
ectForm
osa
with
thePh
ilipp
ines
have
been
seen
inerup
tion.In
thislatter
grou
pno
less
than
nine
teen
lofty
insulated
conicalm
ountains,allcalledin
thecoun
try‘volcane
s,’areen
umerated
byVo
nBu
ch.”(p.460)
n/a
n/a
32Perrey
(1860)
“1831-Le
volcan
situéàlapo
inte
méridionalede
l’îleClaro
Babu
yan(Philippine
s),entre
lesîlesBashi
etLuçon,par19
o27′lat.N
.et119
o42′lon
g.E.,
eutun
eérup
tionsiviolen
te,q
ue,p
ouréchapp
erà
l’embrasem
ent,leshabitantsde
l’îlefurent
forcés
des’e
nfuiravec
laplus
grande
rapidité
(3).Les
petites
îlesBaschi,etlesBabu
yane
s,qu
i,dit
Hum
boldt(4),suivantletémoign
agede
Meyen
,on
tdo
nnéen
core
en1831
lespectacled’un
eviolen
teérup
tionde
flammes...”
[...]
“(3)Landg
rebe,l.c.,p.348,d’après
Meyen,Reise
umdie
Erde,t.II,p.184.DeBuch,l.c.,p.438,m
êmesource.
(4)Cosmos,t.IV,p.
421″
(p.180)
[Translatio
n:“1831-Thevolcanolocatedat
the
southe
rntip
ofClaro
Babu
yanisland
(Philippine
s),
betw
eentheBashiislands
andLuzon,...,
unde
rwen
tan
erup
tionso
violen
tthat,inorde
rto
escape
theblaze,theinhabitantsof
theisland
wereforced
tofleewith
thegreatestrapidity
(3).
Thesm
allB
aschiislands,and
theBabu
yans,w
hich,
states
Hum
boldt(4),accordingto
thetestim
onyof
Meyen
,yielded
in1831
thesigh
tof
aviolen
terup
tionof
flames...
[...]
SVo
nHum
boldt(1859)
Land
greb
e(1855)
VonBu
ch(1836)
[Meyen
(1835)]
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 9 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
“(3)Land
greb
e,l.c.,p.
348,accordingto
Meyen
,Reiseum
dieErde
,v.II,p.
184.DeBu
ch,l.c.,
p.438,samesource.
(4)Cosmos,v.IV,p.
421″]
33Vo
nHum
boldt(1859)
(see
vonHum
boldt1858)
34Vo
nHum
boldt(1858)
“Diekleine
nBaschi-In
seln
unddieBabu
yane
n,welcheno
ch1831
nach
Meyen
’sZe
ugnißeine
nhe
ftigen
Feuerausbrucherlitten,verbinde
nForm
osamitde
nPh
ilipp
inen
...”(v.4,p
.404)
[Translatio
n:“The
smallB
aschi-islands
andtheBabu
yans,
which
accordingto
Meyen
’stestim
onyun
derw
enta
powerfulfiery
erup
tionin
1831,con
nect
Form
osa
with
thePh
ilipp
ines...”]
SMeyen
(1835)
35Land
greb
e(1855)
“8.D
ieInselC
laro
Babu
yan.Sieliegt
inde
rMitte
zwischen
denBashi-Inselnun
dLuzon,ob
erhalb
Cam
iguin.Auf
ihrerSüdspitze,un
ter19
o27′n
.Br.
und119
o42′ö
stl.L.,b
emerkt
man
eine
nmeh
rere
tausen
dFuss
hohe
nVu
lcan,d
ernach
Meyen
’sZe
ugniss
(s.d
essenReiseUm
dieErde
.Bd.
II.S.
184)
imJ.1831
eine
nso
heftigen
Ausbruchhatte,
dass
dieBewoh
nerde
rInselsichzurschn
ellsten
Flucht
genö
thigtsahan,um
dem
sichernVerderbe
nzu
entgeh
en.”(p.348)
[Translatio
n:“8.Babuyan
Claro
island
.Thisislocated
inthemiddlebe
tweentheBashi-islands
andLuzon,
aboveCam
igun
.Atits
southe
rnpo
int...avolcano
severaltho
usandfeet
high
canbe
seen
,which
accordingto
Meyen
’stestim
ony(see
hisVo
yage
arou
ndtheWorld,Volum
eII,Page
184)
unde
rwen
tsuch
apo
werfuleruptionin
1831,thattheinhabitants
oftheisland
hadto
fleeas
quicklyas
possible,in
orde
rto
escape
from
theircertainde
struction.”]
N.B.The
referenceto
v.2,p.
184of
Meyen
(1835)
iseviden
tlyamistakenreferenceto
p.181.Itis
interestingto
note
thede
gree
ofem
bellishmen
twhich
hasbe
enintrod
uced
here:not
onlydidthe
inhabitantshave
tofleetheisland
butthey
had
todo
so‘asqu
icklyas
possible’.
SMeyen
(1835)
36Daube
ny(1848)
“The
volcanicchainisalso
conn
ectedmoreclosely
with
theisland
ofForm
osaby
abu
rningmou
ntain
existin
gin
thegrou
pof
theBabu
janIsland
sinterm
ediate,inwhich
agreaterup
tionthat
occurred
in1831
drovetheinhabitantsfro
mtheisland
.”(p.399)
SVo
nBu
ch(1836)
37Vo
nHoff(1841)
N.B.N
oreferenceto
an1831
erup
tionof
Babu
yan
Claro
(alth
ough
atv.2,p.
182,vonHoffdo
esrefer
n/a
n/a
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 10 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
toMeyen
’s‘Reise
umdieWelt[sic]’).
38Vo
nBu
ch(1836)
“17o
Volcan
del’îlede
Babu
jan,
Lat.19
o27’N
.;Long
.119
o42′1/4.E.d
eParis.C
evolcan
quia
quelqu
esmillepied
sde
hauteur,est.situédans
lapartieou
estde
l’île.U
negrande
érup
tionqu
ieut
lieuen
1831,força
leshabitantsàpren
drelafuite
etàabando
nner
l’île(M
eyen
,Voyage,II,181).”(p.438)
[Translatio
n:“17
oVo
lcanoon
theisland
ofBabu
jan,...This
volcano,which
issomeseveraltho
usandfeet
high
,is
locatedat
thewestern
endof
theisland
.Agreaterup
tion,
which
took
placein
1831,forcedtheinhabitantsto
take
fligh
tandabando
ntheisland
(Meyen
,Voyage,II,181).”]
SMeyen
(1835)
39Meyen
(1835)
“Inde
rNacht
zum
7ten
Aug
ustnähe
rten
wirun
sde
nBashee-In
seln,d
eren
Läng
eno
chaufa
llenKarten
,diewir
anBo
rdde
rPrinzess
hatten
,verschied
enange
gebe
nwar.
WirwähltendieStrasseBalingtangzurDurchfahrtun
dhatten
amfolgen
denMorge
ndieInselB
abuyan
zur
Linken
,und
dieInselB
alingtangzurRechtenim
Gesicht.
DieBergevonBabu
yankönn
eneinige
TausandFuss
anHöh
eüb
ersteige
n,ihre
westlicheSpitzebildet
eine
nschroffenKege
lberg,
derwahrscheinlichde
rVu
lcan
ist,
welcher
noch
vorkurzer
ZeitdieBewoh
nerde
rInselzur
Flucht
getriebe
nhatte.DieBalingtang-Inselh
atin
ihre
Nähesehr
merkw
ürdigge
staltete
Klippe
n…”(v.2,p
.181)
[Translatio
n:“Duringthenigh
tbe
fore
the7thAug
ust,we
approached
theBashee-Island
s,thelatitud
eof
which
was
recorded
differentlyon
allthe
mapsaboard
the
Princess.W
echoseto
approach
throug
htheBalingtang
Straits
and,
onthefollowingmorning
,had
theIsland
ofBabu
yanin
view
ontheleftandtheIsland
ofBalingtang
ontherig
ht.The
mou
ntains
ofBabu
yancouldexceed
afew
thou
sand
feet
inhe
ight,the
irwestern
peak
form
ing
asteepcone
,which
isprob
ablythevolcanowhich
only
ashorttim
eagohadcaused
theinhabitantsof
theIsland
toflee.Balingtangisland
hassomestrang
elyshaped
rocks
inits
vicinity…”]
N.B.O
nhisapproach
toBabu
yanClaro
island
,Meyen
repo
rted
theob
servationof
asolarhalo
andan
extend
edtw
iligh
t:“Am
3ten
Aug
ust…
KurzvorMittags-Ze
it,alsun
sdie
Sonn
efastim
Zenith
stand,
bildetesich
einDun
strin
gum
dieselbe
,dessenRadius
211/2o
betrug
;dieFarbede
sRing
eswar
nichtso
bestim
mt,wiedieeine
sRege
nbog
ens,
undim
Inne
rnde
rRing
esbe
fand
sich
eine
Wolkenm
asse,
welchedu
nklerwar,alsdiede
sum
gebe
nden
Him
mels,
durchwelchewirdieSonn
ekaum
durchseh
enkonn
ten.
Esbe
fand
sich
Niemandan
Bord
desSchiffes,de
mein
solche
rSonn
en-Ring,
welcher
etwas
Aeh
nlichkeitmitde
m
P/S
n/a
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 11 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
soge
nann
tenHofede
sMon
deshatte,zu
Gesicht
gekommen
war.”(v.2,p
p.180–181)
[Translatio
n:“Onthe3rdAug
ust…
Shortly
before
Mid-day,
with
theSunalmostat
theZe
nith
forus,a
hazy
Ring
appe
ared
arou
ndthesame,who
seradius
was
211/2o;the
colour
oftheRing
was
notso
well-d
efined
asthat
ofaRainbo
w,and
inside
theRing
therewas
locateda
Cloud
-masswhich
was
darker
than
that
ofthe
surrou
ndingsky,throug
hwhich
wecouldhardlysee
theSun.Therewas
no-one
onbo
ardtheShip
who
hadob
served
such
aSun-Ring
before,w
hich
hadsome
similaritywith
theso-calledMoo
nHalo.”]
“Auchwurde
indiesen
Tage
neine
Däm
merun
gbe
merkt,
diebe
inaheeine
Stun
denach
Sonn
en-Untergang
anhielt,
woran
woh
ldienied
ereDeclinationde
rSonn
e,nämlich
gerade
16o,d
engrössten
Anthe
ilhatte;diese
Däm
merun
gwurde
aber
auch
nurwen
igeTage
hind
urch
beob
achtet.”(v.2,p
.181)
[Translatio
n:“A
Twiligh
twas
also
expe
rienced
inthese
days
which
continuedalmostan
hour
afterSun-set,
which
was
mainlycaused
bythelow
declinationof
the
Sun,namely16
o;thisTw
iligh
twas
onlyob
served
fora
few
days
however.”]
Asolarhalo
know
nas
a‘Bisho
p’sRing
’issometim
esob
served
afteravolcanicerup
tion(M
eine
land
Meine
l1983).C
ausedby
thediffractio
nof
sunlight
byvolcanog
enicaerosolp
articles,ittypically
appe
arsas
abrighter
whitish-blue
disc
surrou
ndingthesun,
enclosed
byadimmer
redd
ish-brow
nrin
g:the
inne
randou
terradius
oftherin
gvariesby
several
degreesde
pend
ingon
theparticular
size
distrib
ution
oftheaerosolb
utaveragevalues
arec.10-11o
and
22-23o
respectively(Sym
ons1888;M
eine
land
Meine
l1983).M
eyen
’sde
scrip
tionseem
s,ho
wever,a
closer
match
toamorecommon
22osolarhalo.
Causedby
therefractionof
sunlight
(ormoo
nlight)b
yatmosph
ericice-crystals,thisappe
arsas
abrighter
rainbo
w-like
arcarou
ndadimmer
portionen
closing
thesun,with
awelld
efined
redd
ishinne
rradius
at21.7oextend
ingou
twardto
amorediffu
sebluish-w
hite
edge
(Lynch
andLiving
ston
2001).Thecircum
scrib
ed22
osolarhalo
which
isob
served
athigh
solarelevations
isparticularlypron
ounced
(Kön
nen2015).Theextend
edtw
iligh
tappe
arsto
bean
observationof
theun
usual
atmosph
ericop
ticalph
enom
enabe
ing
contem
porane
ouslyob
served
elsewhe
rein
theworld
atthetim
e(asmen
tione
din
theIntrod
uctio
n)bu
tis
thereforeno
tlocaltoBabu
yanClaro
island
oreven
toEastAsia(Arago
1832;Kiessling1888;Sym
ons1888).
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 12 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
40Horsburgh
(1817)
“CLA
ROBA
BUYA
N,orOLD
BABU
YAN,inlat.19
o37’N
.,lon.122o
17′E.,distantabou
t10
leaguesto
the
eastwardof
Calayan,isthemostno
rthe
rlyandhigh
est
oftheseisland
s,in
extent
abou
t2or
21/2leagues.
Thereisareef
projectin
gfro
mtheWesten
dof
theisland
,andthemou
nton
thispartisavolcano;be
twixtwhich,
andthemou
ntains
ontheeasternpart,the
reisaconcave
curvein
theform
ofacrescent,w
henview
edfro
mthe
northw
ardor
southw
ard;
butwhe
ntheisland
isseen
atagreatdistance
from
theeastward,
itappe
arsas
one
roun
dmou
ntain,with
ade
tached
hummockto
the
northw
ard.”(p.328)
n/a
n/a
41DeSalazar(1742)
“CAP.XX
III.FUNDACIONDELA
MISSIONde
Battanes,
ymuertede
losPadres
Fr.M
athe
oGon
çalezyFr.
Juan
Rois...Elaño
de1680...elaño
sigu
iente,...H
aban
sumam
ente
afligidos,y
atem
orizados
conelmucho
sueg
o,pied
ras,ycenizas,qu
eactualmen
tearrojaba
desiun
Volcan,q
ueay
enun
mon
tealto
dedicha
Isla,q
ueàtodo
scausabaterribleho
rror,y
espanto;
yconlaocasionde
lape
na,enqu
ese
hallabanles
comen
zòàpred
icar
elPadreFr.M
athe
o,explicando
les
laspe
nasde
elInferno,ylo
incompreh
ensiblede
los
torm
entos,qu
ehande
pade
cerloscond
enados
por
unaeternidad,
abrassando
seen
susvorazesllamas,
espe
cialmen
telosqu
esien
doChristiano
s,avian
apostatado
delaFeè,yeran
causade
quese
cond
enassensushijos,ynietos,p
ortene
rlosen
aquella
Isla,tan
apartado
sde
lavista,ycommun
icacion
deelMinistro,qu
epu
diesse
doctrin
arlos,ybautizarlos.
Estand
oactualam
ente
pred
icando
elPadreFr.
Mathe
o,eragrande
elestruend
o,yruidode
elVo
lcan,com
ode
gruessos
tiros
deartilleria,con
loqu
alfuetangrande
laconm
ocion,qu
ela
doctrin
ade
elPadrecausòen
todo
sellos,qu
earrassados
enlagrim
assusojos,d
ieronclarissimas
muestrasde
ungrande
arrepe
ntim
ientode
sus
culpas,y
serin
dieron
àlavoluntad
deelPadreFr.
Mathe
o,de
term
inando
sàde
xaraquella
Isla,y
accompañaraldichoReligioso,p
araqu
elos
restiru
iesseàlaIglesia,comolo
executaron
puntualm
ente,sin
qued
arni
unosolo
entoda
laIsla.VinoseelPadreconellosàCagayan...”
(pp.
518–520)
[Translatio
n(M
ontseManzano
Fernande
z):“Chapter
XXIII.Fou
ndationof
theMission
ofBattanes,and
deathof
theFathersFr.M
athe
oGon
çalezand
Fr.JuanRo
is….Year1680…thefollowingyear…
Peop
lewereworriedandfrigh
tene
dby
avolcano,
which
was
ontopof
ahigh
mou
ntainandthat
n/a
n/a
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 13 of 21
Table
1Historicalsourcesanalysed
forthe1831
erup
tionof
Babu
yanClaro.The
sourcesarelistedin
reverseyear
orde
r.Alltranslations
areon
eof
theauthor’s(CG)ow
nexcept
forthetranslationof
source
no.41(Con
tinued)
No.
Source
Text
Source
Type
:Prim
ary/Second
ary
Earlier
source(s)iden
tified.
was
throwingou
tfire,rocksandash.Thisvolcano
caused
everyone
adreadful
horror.W
iththeoccasion
oftheirsadn
ess,Father
Fr.M
athe
ostartedpreaching
tothem
,explainingthepu
nishmen
tsof
Hell,andthe
incompreh
ensibletorm
entsthat
thosecond
emne
dforeternity
wou
lden
dure,b
urning
invoraciou
sflames.Especially
thosewho
wereChristians
andhad
abando
ned(had
apostatized
from)theirfaith
.For
thisreason
they
hadalso
cond
emne
dtheirchildren
andgrandchildren,andforhaving
them
isolated
ontheisland
,far
from
thesigh
tandthereachof
aMinisterwho
couldindo
ctrin
ateandbaptisethem
.One
day,whe
nFather
Fr.M
athe
owas
preaching,
therewas
ahu
gebo
omandno
isefro
mthe
volcano,as
ifitwas
heavyartillery
fire.Peop
lewere
somoved
bythepreachingfro
mthepriestthat,
with
theireyes
fullof
tears,they
show
edvery
clear
sign
sof
agreatrepe
ntance
fortheirsins,and
did
whatFather
Mathe
owanted.
They
werede
term
ined
toleavethat
Island
,and
toaccompany
thepriest,so
that
they
couldbe
includ
edin
theChu
rchagain.
They
leftstraight
away
andtherewas
noon
elefton
thewho
leisland
.Fathe
rFr.M
athe
owen
twith
them
toCagayan…”]
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 14 of 21
for the inhabitants between the observed phenomena andthe torments of those condemned to Hell, whereuponthey all decided to return with the priest to the mainlandin order to remain in communion with the Church.Whether this is a wholly objective account is unclear.Based on the historical and genealogical research that shehas conducted with the Ibatan people living on BabuyanClaro, Maree (2005) also suggests that the 1681 eruptionled to the depopulation of the island and that it remaineduninhabited thereafter until the second half of the nine-teenth century. Additional research will be necessary toinvestigate this evidence further. Clearly, it would seemdoubtful that Meyen (1835) would knowingly have con-sidered a span of 150 years to be ‘only a short time ago’but whether the unacknowledged source from which hegleaned his information reliably represented the date ofthe event described is as yet unknown.For present purposes, it can be concluded that
Meyen’s (1835) account does not represent a primarysource and cannot provide any evidence for an eruptionof either volcano on Babuyan Claro island in 1831.
The 1831 eruption of Babuyan Claro in the later literatureIf this is the case, the question arises as to how an1831 eruption of Babuyan Claro came to appear in thelater literature and, in particular, how it came to berepresented with a VEI of 4? and Magnitude of 4.7
(Crosweller et al. 2012; GVP 2013). Inverting the set ofroutes from the present day back to Meyen (1835)(Fig. 2) suggests several possible pathways from 1831forward to the present day. In fact, the present day repre-sentation of the 1831 eruption can plausibly be ex-plained taking into account the steps taken by just twoauthors.Leopold von Buch published an eruption catalogue in
1836, one year after the publication of Meyen (1835). Heincluded the following entry: “Volcano on the island ofBabujan [sic]...This volcano, which is some several thou-sand feet high, is located at the western end of the island.A great eruption, which took place in 1831, forced the in-habitants to take flight and abandon the island (Meyen,Voyage, II, 181).” (Von Buch 1836; Table 1). Meyen’s 1835account is the only source that Von Buch cites to supportthis entry and yet the two are markedly different. VonBuch evidently regarded the passage as pointing to avolcanic eruption and seems to have made the follow-ing implicit assumptions: (A1) that it must have been a‘great’ eruption, otherwise the inhabitants would nothave fled; and (A2) that ‘a short time ago’ must arbitrarilymean it took place in 1831. Von Buch’s (1836) cataloguewas influential and, based on this interpretation of Meyen’saccount, an entry for a fictitious ‘great’ eruption onBabuyan Claro island in 1831 was widely included inthe subsequent literature.
Fig. 2 Network of routes traced back through the sources for the 1831 eruption of Babuyan Claro. The arrows indicate the citation of an earlier source
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 15 of 21
Karl Sapper published an eruption catalogue in 1917.When he was satisfied there was sufficient evidence,Sapper categorised a number of historical eruptions bytheir products (lava and/or tephra) and their volume(> 0.1 km3 and > 1 km3). Sapper also cited Meyen’s 1835account but, reflecting Von Buch’s interpretation, he tookthe existence of a ‘great’ (or ‘powerful’) eruption of ‘Babu-yan Claro’ in 1831 as a fact (Sapper 1917; Table 1). On thebasis of his reading of the Report of the Krakatoa Com-mittee of the Royal Society (Symons 1888), however, hetook a further step. Part IV, section V of that Report pre-sents a list of observations of unusual atmospheric opticalphenomena over the period 1500–1886, accompanied bya list of historical eruptions. In the case of 1831, alongsidethe unusual atmospheric optical phenomena seen inAugust, September and October 1831, six eruptions werelisted including that of Babuyan Claro (“Babujan Islands(Great eruption)”) (Symons 1888). The Report did not ex-plicitly discuss the attribution of the phenomena to oneeruption or another. Sapper, however, explicitly stated a
further assumption (A3) that the eruption of BabuyanClaro could have contributed to the unusual atmos-pheric optical phenomena observed in Europe (in August,September and October 1831) (Sapper 1917; Table 1) onthe basis of which he assigned it a commensurate tephravolume of 0.1 to 1 km3 (Sapper 1917, Table 1). This vol-ume estimate has been widely used in subsequent quanti-tative treatments of the eruption.For example, erupted volume (lava and/or tephra) is a
key determinant in assigning a value for the VolcanicExplosivity Index (VEI): volumes of 0.01 to 0.1 km3 arecorrelated with a VEI of 3 and 0.1 to 1 km3 with a VEIof 4 (Newhall and Self 1982). Sapper’s (1917) volumeswere used to assign VEI values, although they were treatedas ‘rough estimates’ and were not mechanistically mapped:a number of early nineteenth century eruptions to whichSapper had assigned a 0.1–1 km3 volume have been vari-ously assigned VEI values of 3, 3? and 4 (Simkin et al. 1981;Newhall and Self 1982). The 1831 event was initially treatedas an eruption of Smith volcano and assigned a VEI = 3?
Fig. 3 The re-constructed course of the Prinzess Louise passing Babuyan Claro island in August 1831. The use of this static ArcGIS map image ispermitted in academic publications (including research journals) with the following source attribution: Esri, HERE, De Lorme, MapmyIndia, (c)OpenStreetMap contributors, and the GIS user community. (https://doc.arcgis.com/en/arcgis-online/reference/static-maps.htm, accessed 22/02/2018)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 16 of 21
(Simkin et al. 1981). It was subsequently reclassified as aneruption of Babuyan Claro volcano (COMVOL 1981;Simkin and Siebert 1994) with a VEI of 4? (Simkin andSiebert 1994), bringing the value into line with Sapper’s0.1–1 km3 volume estimate and assigning to BabuyanClaro the largest VEI value of any eruption listed in 1831.It is noteworthy that the reclassification was contempor-ary with Zielinski et al.’s (1994) identification of thiseruption as the source of the large magnitude Greenlandsulphate peak. A VEI of 4? continues to be cited in theGVP database (GVP 2013, although see the accompanyingnote in Table 1).Erupted volume also determines the Magnitude (M) of
explosive eruptions, defined as (Pyle 2000):
M ¼ log10 mass of erupted tephra or lava kgð Þð Þ‐7
The LaMEVE database lists a Magnitude of 4.7 for thiseruption, which is consistent with taking the mid-pointof Sapper’s 0.1–1 km3 volume and using a default tephradensity of 1000 kg m− 3 to obtain a mass of 5 × 1011 kg(Crosweller et al. 2012). The VEI of 4? and Magnitude of
4.7 (Crosweller et al. 2012; GVP 2013) are therefore es-sentially re-statements of Sapper’s (1917) 0.1–1 km3 esti-mate for tephra volume.
The 1831 eruption of Babuyan Claro as a false eruptionOur analysis shows that there is no reason to believethat there was an 1831 eruption of Babuyan Claro. Al-though Meyen’s (1835) account has long been treated asthe single primary source for an 1831 eruption of BabuyanClaro, in fact it provides no evidence of any such eruptionand, indeed, it is possible that it mistakenly refers to anevent as far back as 1681. The records of such an eruptionin the present-day literature can be explained as the resultof Von Buch’s (1836) and Sapper’s (1917) mistaken assump-tions about this account. These results are summarised inFig. 5. We therefore suggest that the 1831 eruption ofBabuyan Claro is a false event and that the records of itin the present-day literature are erroneous, includingthe VEI of 4? listed in the GVP database (GVP 2013)and the Magnitude of 4.7 listed in the LaMEVE database(Crosweller et al. 2012).
Fig. 4 The volcanoes of Babuyan Claro island. Image reproduced with permission: Jonathan Torgovnik / Getty Images News / Getty Images. Smithvolcano, in the foreground (known locally as ‘Pokis’, meaning ‘bald’ or alternatively as ‘Mt. Babuyan’), underwent a series of eruptions between 1907and 1924 (Maree 2005; GVP 2013). Babuyan Claro volcano (‘Chinteb a Wasay’, meaning ‘cut of the axe’ or alternatively ‘Mt. Pangasun’) is in the middledistance (Maree 2005; GVP 2013)
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 17 of 21
Consequences for volcanology and climatologyDiscounting the 1831 eruption, the remaining historicaleruptions of volcanoes on Babuyan Claro island listed inthe GVP database comprise, for Babuyan Claro volcano,1860 (VEI = 2) and 1913 (VEI =2, uncertain) and forSmith volcano, 1652 (VEI =3) and 1907–1924 (five erup-tions, all VEI = 2) (GVP 2013). The modest eruption re-ported by de Salazar (1742) in 1681 is not listed. In theabsence of a historical eruption with a VEI ≥ 4, BabuyanClaro might not be as violently explosive as previouslythought: it may thus have a lower potential for triggeringtsunamigenic hazards (Paris et al. 2014) and its inclusionin the LaMEVE database will no longer be warranted.Neither will there be any evidence to suggest that Babu-yan Claro appears to form ‘part of a high sulphur produ-cing system’ (Zielinski 2000).The mis-identification of an eruption of Babuyan Claro
as the source of the 1831 stratospheric sulphate aerosolwill have hidden its actual source: at least one alternativeeruption will have instead produced the Krakatoa-likeunusual atmospheric optical phenomena observed aroundthe world in August, September and October 1831(Arago 1832; Kiessling 1888; Symons 1888), the surfacetemperature anomalies which occurred between 1831and 1833 (White et al. 1997; Shindell et al. 2004; Fischeret al. 2007; McCarroll et al. 2013) and the large magnitudeGreenland sulphate peak deposited during 1831–1833(Zielinski et al. 1994; Gao et al. 2008; Sigl et al. 2013).A small magnitude sulphate peak resulting from de-
position during 1831–1833 has also been reported inice-cores from Antarctica (Sigl et al. 2013). Although thedetection of near synchronous (within c. 1 year) sulphatepeaks in both Greenland and Antarctic ice-cores suggestsa single low-latitude (tropical) eruption, as was thought tobe the case with Babuyan Claro, another possibility is that
the sulphate peaks are the result of independent erup-tions higher in the northern and southern hemispheres(Sigl et al. 2013). It has been suggested, for example,that the timing of the Antarctic sulphate peak insteadlikely points to a local Antarctic eruption in 1833 (Crowleyand Unterman 2013). The alternative source of theGreenland sulphate peak could therefore be located at amid- or high- latitude site in the northern hemisphere.If Babuyan Claro is discounted, the next largest magni-tude eruptions listed for 1831 have a VEI of 3 (GVP2013): Campi Flegrei Mar Sicilia, off the south coast ofSicily (37.1o N.) (also known as Ferdinandea, Giulia (Julia)and Graham Island); Guagua Pichincha, Ecuador (0.1o S.);and Mount St. Helens, U.S.A. (46.2o N.). A VEI of 3 isassociated with only a ‘possible’ stratospheric injectionof eruption products (Newhall and Self 1982) but this ismore likely to happen at a mid- or high- latitude sitethan a low latitude site given the decrease in height ofthe tropopause from c. 15–17 km at the equator to c.8–9 km at the poles: it has been estimated, for example,that the columns of some 23% of eruptions at mid- orhigh- latitude sites with a VEI of 3 may penetrate thetropopause (Pyle et al. 1996). Whether one of theseknown 1831 eruptions could be the source of theGreenland sulphate peak or whether an as yet unknowneruption is responsible is the subject of continuing work.Although a detailed discussion is beyond the scope of
this paper, a change of source eruption for the Greenlandsulphate peak from one at a low-latitude site to one at amid- or high- latitude site in the northern hemispherecould have quantitative consequences for the correctrepresentation of the 1831 stratospheric sulphate aerosolin climate models. The mass (and therefore the forcingeffect) of the 1831 stratospheric sulphate aerosol is typ-ically reconstructed by ‘scaling up’ the magnitude of the
Fig. 5 The suggested (pre-) history of the 1831 eruption of Babuyan Claro
Garrison et al. Journal of Applied Volcanology (2018) 7:8 Page 18 of 21
Greenland sulphate peak (Zielinski 1995; Gao et al. 2008;Arfeuille et al. 2014; Toohey and Sigl 2017). The choice of‘scaling factor’ depends on the geographical location(latitude) of the assumed source eruption. Substitutinga mid-latitude site in the northern hemisphere insteadof the low-latitude site of Babuyan Claro, for example,would be expected to reduce the reconstructed mass byat least 25% (Zielinski 1995; Toohey and Sigl 2017).The Babuyan Claro example is therefore distinct from
other examples of misattributed eruptions where a climateimpacting stratospheric sulphate aerosol has been produced,but where the change in source location involves only asmall distance at similar latitude. For example, a VEI 5eruption in 1641 (GVP 2013), which produced an even lar-ger Greenland sulphate peak than that in 1831 (Zielinski etal. 1994; Sigl et al. 2013), had previously been attributed toAwu, in Indonesia, but Delfin et al. (1997) established thatit had taken place at Parker volcano, also in thePhilippines, only c. 300 km away.
ConclusionsThe 1831 eruption of Babuyan Claro is regarded as one ofthe most significant volcanic climate forcing events of thenineteenth century (Zielinski 1995; Arfeuille et al. 2014;Toohey and Sigl 2017). However, our analysis shows thatthere is no reason to believe that there was an eruption ofBabuyan Claro in 1831. The historical account whichhas long been treated as the single primary source forthis eruption, Meyen (1835), in fact provides no evidence ofany such eruption. The records of an 1831 eruption ofBabuyan Claro in the present-day literature can be ex-plained as the result of Von Buch’s (1835) and Sapper’s(1917) mistaken assumptions about this account. Wetherefore suggest that the 1831 eruption of BabuyanClaro is a false event and that its records in the present-day literature are erroneous, including the VEI of 4? listedin the GVP database (GVP 2013) and the Magnitude of 4.7listed in the LaMEVE database (Crosweller et al. 2012).The literature on false or misattributed eruptions is
comparatively sparse. Two recent examples are Guidoboni(2010), discussing an example dating to 1198 which hadbeen assigned a VEI of 1 and the above-discussed Delfinet al. (1997). The Babuyan Claro example therefore repre-sents a significant further example of recent date and largemagnitude. In the absence of a historical eruption with aVEI ≥ 4, the hazard assessment of Babuyan Claro volcanowill have to be re-evaluated and, for example, the inclu-sion of Babuyan Claro in the LaMEVE database will nolonger be warranted.At least one alternative eruption, potentially at a mid-
or high- latitude site in the northern hemisphere and witha high sulphur yield, will have to be identified as the sourceof the 1831 stratospheric sulphate aerosol. Such a changeof source eruption could have quantitative consequences
for the correct representation of the 1831 stratosphericsulphate aerosol in climate models. The Babuyan Claro ex-ample thus emphasises the potential for misattributederuptions to have a significant impact on both volcanologyand climatology and reinforces Guidoboni’s (2010) call forthe careful analysis of primary historical sources in volcan-ology. Whether one of the remaining historical eruptionslisted for 1831 in the GVP database could be the source orwhether an as yet unknown eruption is responsible is thesubject of continuing work.
AbbreviationsCAVW: Catalogue of the Active Volcanoes of the World; CDSB: CompleteDictionary of Scientific Biography; COMVOL: (Philippines) Commission onVolcanology; GVP: Global Volcanism Program; LaMEVE: Large MagnitudeExplosive Volcanic Eruptions; PHIVOLCS: Philippine Institute of Volcanologyand Seismology; VEI: Volcanic Explosivity Index
AcknowledgmentsWe would like to thank Montse Manzano Fernandez for providing thetranslation of de Salazar (1742), Ben Andrews (Smithsonian Institution) forinformation regarding the GVP database and Danielle Charlton (UCL HazardCentre) for assistance with the preparation of Fig. 3. We would also like tothank Russell Blong, an anonymous second reviewer and Christopher Newhallfor the improvements to the manuscript which resulted from their comments.
FundingThis work was self-funded (CG).
Availability of data and materialsAll data generated or analysed during this study are included in thispublished article.
Authors’ contributionsCG carried out the analysis presented in this study and drafted the manuscript.CK and SE critically reviewed the manuscript and provided guidance andexpertise on the volcanological context. All authors read and approved the finalmanuscript.
Competing interestsThe authors declare that they have no competing interests.
Publisher’s NoteSpringer Nature remains neutral with regard to jurisdictional claims inpublished maps and institutional affiliations.
Received: 27 February 2018 Accepted: 21 August 2018
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