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Author's personal copy
Journal
of
Geodynamics
66 (2013) 1–
12
Contents
lists
available
at
SciVerse
ScienceDirect
Journal
of
Geodynamics
j
ourna
l
ho
me
page:
http://www.elsevier.com/locate/jog
Analysis
of
vertical
movements
in
eastern
Sicily
and
southern
Calabria
(Italy)
through
geodetic
leveling
data
Cecilia
Rita
Spampinatoa,
Carla
Braitenbergb,
Carmelo
Monacoa,∗,
Giovanni
Scicchitanoa,c
aDipartimento
di
Scienze
Biologiche,
Geologiche
e
Ambientali,
Università
degli
Studi
di
Catania,
Italy
bDipartimento
di
Matematica
e
Geoscienze,
Università
degli
Studi
di
Trieste,
Italy
cStudio
Geologi
Associati
T.S.T.
Via
Galliano,
157,
95045,
Misterbianco,
Catania,
Italy
a
r
t
i
c
l
e
i
n
f
o
Article
history:
Received
10
September
2012
Received
in
revised
form
19
December
2012
Accepted
19
December
2012
Available online xxx
Keywords:
Calabrian
arc
Sicily
Geodetic
leveling
Vertical
movements
a
b
s
t
r
a
c
t
The
analysis
of
repeated
high
precision
leveling
observations
during
the
last
40
years
along
lines
of
the
Italian
fundamental
network
allowed
us
to
estimate
very
recent
vertical
movements
in
eastern
Sicily
and
southern
Calabria
(Italy).
The
network
is
measured
by
the
Italian
Istituto
Geografico
Militare
(IGM)
and
we
have
analyzed
three
leveling
lines.
Because
of
the
lack
of
an
absolute
reference
datum,
we
have
conducted
the
analyses
in
terms
of
relative
elevation
changes
compared
to
reference
benchmarks.
Although
the
processing
of
the
different
time
series
obtained
from
the
high
precision
leveling
has
allowed
us
to
estimate
only
relative
rates,
their
extreme
accuracy,
together
with
the
large
extension
of
networks,
makes
this
type
of
measurement
fundamental
for
the
estimate
of
recent
vertical
deformation.
In
addition,
correlating
instrumental
and
geological
data
makes
it
possible
to
identify
active
tectonic
structures
whose
elastic
strain
accumulation
could
be
responsible
for
vertical
deformation.
In
particular,
vertical
motion
can
be
related
to
the
activity
of
a
W-E
trending
fault
separating
the
Catania
Plain
from
the
Hyblean
Plateau
in
southeastern
Sicily,
a
N-S
trending
normal
fault
occurring
north
of
the
Messina
town
and
the
NE-SW
trending
Scilla
normal
fault
in
south-western
Calabria.
The
last
two
are
located
on
the
sides
of
the
Messina
Straits,
an
area
of
broad
interest
for
the
planning
of
the
single-span
bridge
between
Sicily
and
mainland
Italy.
© 2012 Elsevier Ltd. All rights reserved.
1.
Introduction
The
Late
Quaternary
tectonic
evolution
of
eastern
Sicily
and
southern
Calabria
(Italy,
Fig.
1)
has
been
characterized
by
strong
vertical
movements
that
have
been
recorded
by
uplifted
marine
terraces
and
palaeo-shorelines.
Long
term
uplift
has
been
con-
strained
by
the
elevation
of
the
last
interglacial
(125
ka,
MIS
5.5)
terraces
(Ferranti
et
al.,
2006)
and
has
been
related
to
regional
processes
to
which
faulting-related
deformation
is
added
along
fault-controlled
coastal
segments
(Westaway,
1993).
The
uplift
pattern
of
the
125
ka
terrace
is
replicated
by
the
Holocene
paleo-
shorelines.
In
particular,
in
north-eastern
Sicily
and
southern
Calabria
data
on
vertical
movements
during
the
Holocene
have
been
obtained
by
measurement
and
radiometric
dating
of
biologi-
cal
and
morphological
markers
(Stewart
et
al.,
1997;
De
Guidi
et
al.,
2003;
Antonioli
et
al.,
2003,
2006a;
Ferranti
et
al.,
2007;
Scicchitano
et
al.,
2011;
Spampinato
et
al.,
2012).
In
south-eastern
Sicily
data
have
been
obtained
by
analysis
of
boreholes
from
lagoonal
deposits
(Monaco
et
al.,
2004;
Spampinato
et
al.,
2011)
and
by
measures
of
∗Corresponding
author.
Fax:
+39
957195728.
E-mail
address:
cmonaco@unict.it (C.
Monaco).
submerged
archeological
markers
and
of
speleothems
collected
in
karstic
caves
(Scicchitano
et
al.,
2008).
Holocene
vertical
crustal
movements
derived
from
biological,
geomorphologic
or
archeological
markers
have
been
estimated
using
the
predicted
sea
level
as
reference
datum
(e.g.
Lambeck
et
al.,
2004)
but
present
day
precise
geodetic
estimates
are
still
lack-
ing.
Antonioli
et
al.
(2009)
and
Braitenberg
et
al.
(2011)
used
the
differential
sea
level
changes
between
tide
gauges
and
altimetric
satellites
to
estimate
vertical
movements
at
the
tide
gauge
stations
in
Sicily,
finding
that
both
Messina
and
Catania
have
been
uplifting
at
similar
rates
with
respect
to
the
stable
Palermo
station.
Never-
theless,
the
authors
pointed
out
that
the
overlapping
time
window
between
tide
gauges
and
altimeter
was
still
short
to
obtain
reliable
vertical
movement
rates
of
the
stations.
The
presently
available
GPS
observations
are
too
short
to
give
reliable
vertical
movements,
as
well
(Mattia
et
al.,
2009,
2012)
In
this
work
we
approach
the
problem
of
estimating
vertical
movements
in
eastern
Sicily
and
southern
Calabria
using
a
network
of
high
precision
leveling
lines
performed
by
the
Italian
Istituto
Geografico
Militare
(IGM).
Determination
of
vertical
deformation
by
leveling
data
has
some
advantages:
(i)
it
is
the
only
geodetic
dataset
regarding
vertical
movements
that
spans
back
in
time
to
the
past
50–100
years;
(ii)
the
resolution
in
evaluating
the
vertical
0264-3707/$
–
see
front
matter ©
2012 Elsevier Ltd. All rights reserved.
http://dx.doi.org/10.1016/j.jog.2012.12.002
Author's personal copy
2C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12
Fig.
1.
Tectonic
sketch
map
of
southern
Calabria
and
eastern
Sicily
(after
Monaco
and
Tortorici,
2000;
modified).
Crustal
seismicity
(H
<
35
km)
since
1000
AD
is
also
shown
(data
from
Gasparini
et
al.,
1982;
Postpischl,
1985;
Anderson
and
Jackson,
1987;
Boschi
et
al.,
1995).
component
of
motion
is
one
order
of
magnitude
better
than
GPS
estimates;
and
(iii)
anyhow,
no
comparable
sampling
of
active
regions
(1
benchmark
per
km)
is
presently
available
from
GPS
net-
works
in
Italy.
On
the
contrary,
the
main
disadvantage
of
leveling
measurements
is
the
lack
of
an
absolute
reference
datum,
and
only
relative
motion
can
be
precisely
determined
by
comparative
level-
ing
data
(Bomford,
1971).
However,
we
show
that
cross
analysis
of
instrumental
data
with
structural
geological
surveys
may
reveal
the
activity
of
tectonic
structures,
supposedly
responsible
for
the
vertical
deformation
recorded
in
the
areas
crossed
by
leveling
lines.
Repeated
leveling
has
been
used
in
different
locations
to
successfully
determine
tectonic
and
anthropogenic
vertical
move-
ments.
Rózsa
et
al.
(2005)
relate
rate
changes
to
the
crossing
of
some
main
faults
in
the
upper
Rhine
graben
in
a
slow
moving
tec-
tonic
environment
with
mean
movement
rates
in
60
years
up
to
0.25
mm/yr.
The
GPS
observations
were
too
short
to
give
signifi-
cant
results
as
rates
were
below
the
1
mm/yr
level.
Grzempowski
et
al.
(2009)
observe
subsidence
of
benchmarks
in
Slesia
(Poland)
which
they
ascribe
to
compaction
of
sediments.
Along
the
coastline
of
the
Eastern
Betic
Cordillera,
SE
Spain,
Gimenez
et
al.
(2009)
ana-
lyzed
the
repeated
leveling
over
a
27
year
time
span
and
found
vertical
movement
rates
near
to
0.2
mm/yr,
which
has
been
esti-
mated
to
be
close
the
precision
of
the
method.
The
rates
were
in
good
agreement
with
the
geologically
determined
rates
based
on
geological
markers.
Short
term
vertical
movement
was
obtained
at
a
fault
by
a
dedicated
repeated
leveling
experiment
near
Izmir,
Turkey
by
Ozener
et
al.
(2012).
Peak
subsidence
rates
up
to
30
cm/yr
in
Northern
Iran
were
observed
with
excellent
agreement
with
both
Interferometric
Synthetic
Aperture
Radar
(InSAR)
and
leveling
and
were
ascribed
to
subsurface
water
withdrawal
(Motagh
et
al.,
2007)
controlled
by
the
presence
of
Alpine
faults
(Anderssohn
et
al.,
2008);
the
acceleration
of
rates
was
shown
by
using
the
older
and
newer
leveling
repetitions.
Drakos
et
al.
(2001)
used
repeated
level-
ing
to
invert
for
the
fault
mechanism
of
a
6.5
magnitude
earthquake.
Repeated
leveling
was
used
to
quantify
subsidence
due
to
magma
injection
and
exploitation
of
a
geothermal
field
over
a
Caldera
in
Eastern
California
(Howle
et
al.,
2003).
Further
recent
studies
using
repeated
leveling
to
obtain
geodynamic
information
over
volcanic
Author's personal copy
C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12 3
Fig.
2.
(a)
The
IGM
high
precision
leveling
network
in
Italy.
(b)
Traces
of
the
three
analyzed
lines
(red
lines).
(For
interpretation
of
the
references
to
color
in
this
figure
legend,
the
reader
is
referred
to
the
web
version
of
this
article.)
areas
were
made
by
Sarychikhina
et
al.
(2011)
and
Poland
et
al.
(2006).
The
Italian
leveling
lines
have
been
used
in
the
Apennines
to
reveal
short-term
vertical
velocities
by
D’Anastasio
et
al.
(2006).
2.
Geological
setting
The
study
areas
are
located
along
the
Calabrian
Arc
and
east-
ern
Sicily
(Fig.
1),
the
most
seismically
active
areas
of
the
central
Mediterranean,
where
the
effects
of
Quaternary
tectonics
are
bet-
ter
preserved.
The
Calabrian
Arc,
which
includes
southern
Calabria
and
north-eastern
Sicily,
connects
the
Apennines
and
the
Sicilian-
Maghrebian
chains
that
developed
during
the
Neogene-Quaternary
Africa–Europe
collision
(Dewey
et
al.,
1989),
and
was
emplaced
to
the
south-east
during
north-westerly
subduction
and
roll-back
of
the
Ionian
slab
(Malinverno
and
Ryan,
1986).
Since
Pliocene
times,
contractional
structures
of
the
inner
part
of
the
orogen
were
superseded
by
extensional
faults,
both
longitudinal
and
transversal
with
respect
to
the
arc,
that
caused
the
fragmentation
into
struc-
tural
highs
and
marine
sedimentary
basins
(Ghisetti
and
Vezzani,
1982).
In
eastern
Sicily
and
Calabria,
Quaternary
extension
at
the
rear
of
the
thrust
belt
has
been
accompanied
by
a
vigorous
uplift
(1–2
mm/yr)
recorded
by
flights
of
marine
terraces
(Westaway,
1993;
Miyauchi
et
al.,
1994;
Ferranti
et
al.,
2006).
The
seismicity
of
the
Calabrian
Arc
and
eastern
Sicily
is
defined
by
the
occurrence
of
both
crustal
(H
<
35
km)
and
subcrustal
(H
>
35
km)
earthquakes.
The
latter
are
located
beneath
the
south-
ern
Tyrrhenian
sea,
reaching
470
km
of
depth
and
depicting
a
slab
dipping
about
45◦toward
NW
(Gasparini
et
al.,
1985;
Anderson
and
Jackson,
1987;
Neri
et
al.,
2012).
Crustal
seismicity
is
defined
by
historical
and
instrumental
earthquakes
(Postpischl,
1985;
Boschi
et
al.,
1995,
1997;
Scarfì
et
al.,
2009).
The
epicentral
distribution
of
the
M
≥
6
earthquakes
(Fig.
1)
outlines
a
seismic
belt
which
runs
along
the
Tyrrhenian
side
of
the
Calabrian
arc
and,
southward,
along
the
Ionian
coast
of
Sicily
and
the
Hyblean
Plateau,
where
active
WNW-ESE
extension
is
documented
by
focal
mechanisms
of
crustal
earthquakes
(Neri
et
al.,
2004;
Pondrelli
et
al.,
2006),
struc-
tural
studies
(Tortorici
et
al.,
1995;
Monaco
et
al.,
1997;
Monaco
and
Tortorici,
2000;
Jacques
et
al.,
2001;
Ferranti
et
al.,
2007),
and
satel-
lite
geodetic
observations
(D’Agostino
and
Selvaggi,
2004;
Mattia
et
al.,
2009;
Palano
et
al.,
2012).
The
southeastern
Sicily
area
(Fig.
1)
is
characterized
by
thick
Mesozoic
to
Quaternary
carbonate
sequences
and
volcanics
form-
ing
the
emerged
foreland
of
the
Siculo-Maghrebian
thrust
belt
(Grasso
and
Lentini,
1982).
This
area,
mostly
constituted
by
the
Hyblean
Plateau,
is
located
on
the
footwall
of
a
large
oblique-
normal
fault
system
which
since
the
Middle
Pleistocene
has
reactivated
the
Malta
Escarpment
(Bianca
et
al.,
1999),
a
Meso-
zoic
boundary
separating
the
continental
domain
from
the
oceanic
crust
of
the
Ionian
basin
(Scandone
et
al.,
1981;
Sartori
et
al.,
1991;
Hirn
et
al.,
1997).
In
this
area,
the
vertical
component
of
deformation
has
been
recorded
by
several
orders
of
Middle-
Upper
Quaternary
marine
terraces
and
paleo-shorelines
(Di
Grande
and
Raimondo,
1982;
Bianca
et
al.,
1999),
which
indicate
uplift
rates
of
about
0.5
mm/yr
during
the
Late
Quaternary
(Scicchitano
et
al.,
2008;
Dutton
et
al.,
2009).
Uplift
rates
gradually
decrease
toward
the
stable
areas
of
the
south-eastern
corner
of
Sicily
(Antonioli
et
al.,
2006b;
Ferranti
et
al.,
2006;
Spampinato
et
al.,
2011).
3.
Leveling
network
For
over
120
years
the
Italian
Istituto
Geografico
Militare
(IGM)
has
repeatedly
measured
the
elevation
along
the
national
leveling
lines
which
cover
the
Italian
peninsula
(Fig.
2a).
The
IGM
leveling
network
has
been
measured
with
high
precision
leveling
tech-
niques,
following
the
International
Geodetic
Association
standards
defined
in
Oslo
in
1948
(Vignal,
1936,
1950)
and
it
is
composed
by
leveling
lines
over
a
total
length
of
14.000
km.
Each
leveling
line
is
defined
by
its
benchmarks,
characterized
by
the
line
number
and
a
consecutive
identification
number.
Benchmarks
are
classi-
fied
into
four
categories:
category
I
or
nodal
benchmark,
located
at
the
vertices
of
the
polygon
network;
category
II
or
fundamen-
tal
benchmark,
located
every
25
km
along
the
line;
category
III
or
main
benchmark,
located
at
the
beginning
and
the
end
of
5
km
long
segments;
category
IV
located
at
a
distance
of
1
km.
For
each
bench-
mark
there
is
a
monograph
where
the
monographic
and
numerical
data
necessary
for
its
finding
and
for
its
use
are
reported.
The
clas-
sification
into
four
categories
has
only
organizational
purposes
and
does
not
affect
the
precision,
which
is
uniform
for
all
benchmarks
(Muller,
1986).
Author's personal copy
4C.R.
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et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12
The
leveling
is
the
most
accurate
method
to
measure
the
height
difference
between
consecutive
points.
To
determine
the
height
of
a
benchmark
it
is
necessary
to
measure
the
difference
in
height
between
this
benchmark
and
another,
whose
altitude
is
known
by
previous
measurements
obtained
from
the
fundamen-
tal
benchmark.
The
procedure
to
determine
the
measurement
of
the
difference
of
level
is
called
geometric
leveling.
Depending
on
the
degree
of
measurement
accuracy,
the
geometric
leveling
comes
classified
as
technical,
precision
and
high
precision.
For
the
study
of
vertical
deformation
it
is
necessary
to
use
the
high
precision
leveling.
The
IGM
high
precision
leveling
standards,
since
1940,
require
for
the
measurement
campaigns:
(a)
double
leveling
between
consecutive
benchmarks,
with
maximum
allowed
discrepancy
between
forward
and
backward
leveling
of
±
2.5 √L
mm,
where
L
is
the
length
of
the
leveled
segment,
in
km,
and
L
<
4
km.
For
L
=
4
km
that
amounts
to
a
maximum
of
4
mm
difference
between
forward
and
backward
leveling.
For
a
length
L
<
50
km
the
max-
imum
allowed
difference
between
the
forward
and
backwards
operation
is
limited
to
1.5
L3/4 mm
length,
which
amounts
to
a
maximum
discrepancy
of
28
mm
for
a
length
of
50
km.
For
lengths
above
50
km
the
discrepancy
is
limited
to
4
L1/2 mm,
which
for
100
km
amounts
to
40
mm;
(b)
equal
number
of
setup
for
forward
and
backward
measurements;
(c)
circuit
closure
with
maximum
admitted
error
of
±2.0 √L
mm,
where
L
is
the
circuit
length
in
km.
For
a
length
of
200
km
the
circuit
closure
tolerance
amounts
to
28
mm;
(d)
instrument
calibration
before
and
after
each
survey;
(e)
maximum
allowed
sight
length
of
50
m;
and
(f)
use
of
invar
rod
and
rod
correction
(Salvioni,
1951;
Muller,
1986).
The
final
precision
of
the
geometric
leveling
is
characterized
by
the
probable
kilometric
error
that
is
obtained
from
the
compen-
sation
of
the
measurements,
through
the
mean
square
error
of
the
level
difference
between
two
leveled
points
1
km
apart
(Muller,
1986).
To
this
the
probable
systematic
error
is
added,
so
the
probable
total
kilometric
error
is
defined
with
=2+
2.
The
expected
error
on
the
level
difference
on
a
line-segment
of
length
L
km
is
√L,
according
to
Vignal
(1936)
and
adopted
at
the
Assembly
of
the
International
Geodetic
Association
in
Oslo
in
1948
(Bul-
letine
geodesique
N◦18,
1950).
In
that
conference
a
high
precision
leveling
was
defined
by
a
kilometric
error
≤2
mm,
and
a
precision
leveling
by
a
kilometric
error
≤6
mm.
For
the
lines
of
the
Italian
high
precision
network
we
are
using,
the
value
of
=
±0.72
mm/km
is
required
and
guaranteed
by
the
IGM
who
have
carried
out
the
high
precision
leveling
(Salvioni,
1957)
for
all
stations
of
the
level-
ing
network.
The
absolute
levels
of
the
stations
were
referred
in
Sicily
to
the
mean
sea
level
in
Catania
in
the
year
1965;
for
the
Ital-
ian
mainland,
including
the
stations
we
consider
for
Calabria,
they
were
referred
to
the
mean
sea
level
in
Genova
in
the
year
1942.
4.
The
high
precision
leveling
lines
When
leveling
data
are
used
for
tectonic
purposes,
it
is
impor-
tant
to
determine
the
magnitude
of
systematic
and
random
error
and
their
propagation
along
a
leveling
line.
Large
system-
atic
errors
are
usually
slope-dependent
and
can
be
detected
by
checking
the
correlation
between
elevation
and
elevation
change
on
the
analyzed
leveling
routes.
The
most
important
sources
of
slope-dependent
errors
are
rod
calibration
and
refraction
errors
(Bomford,
1971).
Rod
calibration
errors
are
usually
detected
by
using
the
method
proposed
by
Stein
(1981).
Refraction
errors
largely
affect
leveling
data
especially
when
setup
length
changes
occur
between
repeated
surveys
(Holdahl,
1981).
In
Italy,
maxi-
mum
allowed
setup
length
has
not
changed
from
1950
until
now,
being
of
50
m.
Moreover,
tests
performed
on
our
data
do
not
show
significant
correlations
between
heights
and
height
changes,
which
usually
indicate
the
presence
of
large
slope
dependent
errors
(Jackson
et
al.,
1981;
Reilinger
and
Brown,
1981;
Stein,
1981).
In
order
to
quantify
random
error
propagation,
it
is
important
to
analyze
the
original
raw
height
data,
but
being
these
not
easily
accessible
in
the
IGM
archive,
we
are
forced
to
use
adjusted
heights
to
define
vertical
movements.
However,
D’Anastasio
et
al.
(2006)
showed
that
the
use
of
adjusted
heights
instead
of
raw
height
data
does
not
affect
elevation
change
values.
In
theory,
the
leveling
lines
give
absolute
values
of
height,
and
the
repeated
leveling
should
give
absolute
vertical
rates,
if
all
leveled
values
are
referred
to
an
absolute
stable
vertical
datum.
A
full
control
on
the
consistency
of
the
absolute
rates
would
require
the
entire
network
to
be
available
with
repeated
measurements
and
to
be
tied
to
a
stable
vertical
datum.
This
information
is
though
not
available,
as
the
repeated
measurements
do
not
cover
the
entire
network
at
the
same
time
and
on
all
stations.
We
prefer
to
have
a
conservative
estimate
of
vertical
rates,
that
is
to
calculate
the
rates
relative
to
one
of
the
benchmarks
of
the
line.
We
are
therefore
not
interested
in
the
absolute
vertical
rates,
but
in
the
relative
rates
along
the
leveled
line.
This
information
is
sufficient
when
investi-
gating
the
correlation
with
the
local
geologic
features,
as
we
are
not
investigating
the
absolute
vertical
movement
with
respect
to
an
external
reference
frame,
as
could
be
sea
level
or
the
ellipsoid,
but
we
determine
the
lateral
inhomogeneities
of
the
vertical
rate.
Therefore,
because
of
the
lack
of
an
absolute
reference
datum,
we
have
conducted
the
analyses
in
terms
of
relative
elevation
changes.
So
we
have
calculated
relative
vertical
rates
using
the
time
elapsed
between
repeated
surveys
of
each
line
or
line
section,
according
to
the
relationship:
i=qt2
i−
qt1
i
(t2
−
t1) (1)
where
qt2
iand qt1
iare
the
altitudes
of
the
i-th
benchmark
measured
during
two
measurement
surveys.
The
i-th
benchmark
elevation
is
closely
linked
to
the
height
of
the
reference
benchmark.
Taking
into
account
that
this
height
is
not
measured
by
method
of
leveling,
and
for
this
reason
may
be
affected
by
an
error,
it
follows
that
this
error
can
lead
to
a
constant
error
along
the
entire
line.
To
avoid
that
the
error
in
the
measurement
of
the
first
benchmark
invalids
the
rate
of
deformation
along
the
line,
in
this
work
we
have
calculated
the
rate
of
deformation
of
the
i-th
benchmark
relative
to
the
rate
of
the
reference
benchmark
and
applying
the
following
relationship:
i=qt2
i−
qt1
i−
qt2
0−
qt1
0
(t2
−
t1) (2)
where
qt2
i,
qt1
i,
qt2
0,
qt1
0are
the
altitudes
of
the
i-th
benchmark
and
reference
benchmark,
respectively,
measured
during
two
measure-
ment
surveys.
This
procedure
does
not
affect
the
analysis
of
the
lateral
changes
of
the
calculated
rates,
but
applies
only
a
static
shift
to
the
lines.
We
are
therefore
sure
that
the
calculated
rates
are
rel-
ative
to
the
reference
benchmark.
If
the
reference
benchmark
is
uplifting,
this
value
will
be
added
to
the
entire
line.
If
it
is
subsid-
ing,
this
value
must
be
subtracted
to
the
entire
line.
In
either
case
the
lateral
changes
we
are
analyzing
relatively
to
the
geological
fea-
tures
will
not
be
affected
and
the
final
results
and
conclusions
will
not
change.
We
estimate
the
standard
deviation
error
on
the
ver-
tical
rate
at
one
benchmark
from
the
equation
(Rozsa
et
al.,
2005;
Gimenez
et
al.,
2009):
i=
0.72
∗li
t2
−
t1mm/yr
(3)
With
lithe
distance
to
the
next
leveled
benchmark
along
the
line,
and
assuming
that
the
expected
error
on
nearby
benchmarks
is
independent
and
of
the
same
order
of
magnitude,
which
is
Author's personal copy
C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12 5
taking
advantage
of
the
fact
that
for
the
lines
we
are
considering
the
distance
between
the
benchmarks
is
near
to
equal.
In
order
to
study
the
vertical
deformation
in
some
areas
of
eastern
Sicily
and
southern
Calabria
during
the
last
40
years,
all
available
high
precision
leveling
lines
were
analyzed.
The
major
part
of
lines
were
only
measured
once,
and
are
lacking
the
repe-
tition,
and
therefore
could
not
be
used
for
the
estimate
of
vertical
movements.
Three
lines
had
been
measured
repeatedly
and
were
useful
for
our
purpose:
Line
108,
Line
92
and
Line
100
(Fig.
2b).
The
last
two
are
very
important
as
they
pass
through
the
sites
that
were
chosen
for
the
pylons
of
the
3
km
long
single-span
bridge
crossing
the
Messina
Straits.
For
each
line
the
elevations
and
the
WGS84
coordinates
of
the
selected
benchmarks,
have
been
extracted
from
IGM
monographs.
Conversion
into
kilometric
coor-
dinates
has
allowed
to
calculate
the
distance
of
each
benchmark
from
the
reference
benchmark.
Before
proceeding
with
the
cal-
culation
of
the
relative
vertical
deformation
rate,
data
have
been
analyzed
in
order
to
evaluate
if
they
were
suffering
by
slope-
dependent
error
(D’Anastasio
et
al.,
2006).
By
plotting
the
heights
of
benchmarks
(abscissa)
with
the
elevation
change
(ordinate)
(Fig.
3),
we
observe
that
there
is
no
linear
relationship
between
the
heights
and
the
heights
change
which
normally
can
indicate
the
presence
of
a
systematic
error
related
to
the
slope
(Jackson
et
al.,
1981;
Reilinger
and
Brown,
1981;
Stein,
1981).
In
the
following,
the
main
characteristics
of
each
line
are
sum-
marized.
4.1.
Line
108
The
Line
108
covers
south-eastern
Sicily
(Fig.
2b)
and
was
mea-
sured
by
IGM
for
the
first
time
in
1970.
It
is
148.403
km
long
and
consists
of
143
benchmarks;
the
nodal
point
from
which
the
line
extends
is
the
number
#No75,
located
near
the
town
of
Ragusa,
whereas
the
last
benchmark
(#143)
is
located
in
the
southern
periphery
of
Catania.
In
order
to
determine
the
relative
vertical
deformation
rate,
at
least
two
measurement
surveys
are
required;
the
benchmarks
from
#No75
to
#106,
were
measured
only
once,
and
were
discarded
for
our
purposes.
We
focused
on
the
line
section
between
the
benchmark
#107
located
near
Augusta
and
the
bench-
mark
#143,
located
in
Catania
(Fig.
4a).
This
segment
is
∼38
km
long
and
has
been
measured
in
two
successive
surveys,
in
1970
and
in
1991.
By
comparing
the
benchmark
heights
measured
in
the
two
surveys,
the
total
elevation
change
that
occurred
in
the
time
interval
between
1970
and
1991has
been
obtained
(Fig.
4b).
The
elevation
changes
range
between
−−33
mm
and
−300
mm,
and
are
much
greater
than
the
expected
errors
on
the
height
differ-
ences,
which
are
near
to
1
mm,
given
that
the
distance
between
benchmarks
is
mostly
below
2
km.
In
order
to
calculate
the
vertical
deformation
rate
of
each
bench-
mark
with
respect
to
the
benchmark
#107
in
the
1970–1991
time
interval,
the
relationship
(2)
has
been
applied.
In
Table
1
the
rel-
ative
rates
of
vertical
deformation
(mm/yr)
for
each
benchmark
are
reported.
In
order
to
identify
the
possible
causes
of
vertical
deformation,
a
schematic
geological
profile
along
the
line
has
been
carried
out
(Fig.
4c).
Geological
data
have
been
obtained
from
the
1:50.000
scale
maps
of
the
Servizio
Geologico
d’Italia
(2009;
2011);
and
have
been
reported
on
a
topographic
profile
drawn
from
a
2
×
2
m
grid
digital
terrain
model
(DTM)
obtained
from
Lidar
flight
(http://www.sitr.regione.sicilia.it/).
4.2.
Line
92
The
Line
92
covers
northern
Sicily
(Fig.
2b)
and
was
measured
by
IGM
for
the
first
time
in
1967.
It
is
229.43
km
long
and
consists
of
221
benchmarks;
the
nodal
point
from
which
the
line
extends
is
the
number
#No68,
located
near
the
town
of
Messina,
whereas
the
last
benchmark
(#221)
is
located
near
the
village
of
Buonfor-
nello.
The
benchmarks
from
#18
to
#221,
measured
only
once,
were
discarded.
We
focused
on
the
line
section
between
the
nodal
benchmark
#No68,
located
near
Messina,
and
the
benchmark
#17
(Fig.
5a).
This
is
∼38
km
long
and
has
been
measured
in
three
dis-
tinct
surveys,
in
1967,
1986
and
2004.
For
this
line
the
three
time
intervals
1967–1986,
1986–2004
and
1967–2004
have
been
examined.
By
comparing
the
bench-
mark
heights
measured
in
the
three
surveys,
the
total
elevation
change
occurred
at
the
considered
time
intervals
has
been
obtained
(Fig.
5b).
With
respect
to
line
108
located
to
the
southwards
and
discussed
above,
the
height
differences
here
are
much
smaller,
between
7
mm
and
−15
mm,
for
the
longest
time
interval.
In
order
to
calculate
the
vertical
deformation
rate
in
the
1967–1986,
1986–2004
and
1967–2004
time
intervals,
the
rela-
tionship
of
equation
2
has
been
applied.
The
vertical
deformation
rates
(mm/yr)
for
each
benchmark
were
calculated
with
respect
to
the
reference
benchmark
#No68
and
are
reported
in
Table
2.
For
the
shortest
time
interval,
less
than
a
decade
long,
the
smaller
vertical
rates
are
at
the
limit
of
resolution.
The
three
rates,
calcu-
lated
over
the
two
successive
intervals
and
over
the
entire
time
interval
are
perfectly
coherent,
enforcing
the
weight
of
the
results.
A
schematic
geological
profile
along
the
line
(Fig.
5c)
allowed
us
to
reconstruct
the
lithological
succession
under
each
benchmark
and
to
identify
the
possible
causes
of
vertical
deformation
(geology
from
Gargano,
1994;
topography
from
a
2
×
2
m
grid
Lidar
flight
DTM
(http://www.sitr.regione.sicilia.it/)
4.3.
Line
100
The
Line
100
has
been
instituted
in
southern
Calabria
(Fig.
2b)
and
measured
by
IGM
for
the
first
time
in
1966.
It
is
134.896
km
long
and
consists
of
129
benchmarks;
the
nodal
point
from
which
the
line
extends
is
the
#No69,
located
near
the
town
of
Reggio
Cala-
bria,
whereas
the
last
benchmark
(#129)
is
located
near
the
village
of
Santa
Eufemia.
The
benchmarks
from
#No69
to
#10
and
from
#33
to
#129,
measured
only
once,
were
discarded.
We
focused
on
the
line
section
between
the
benchmark
#11,
located
near
Reggio
Calabria,
and
the
benchmark
#132P,
located
near
Bagnara
Calabra
(Fig.
6a),
which
is
∼24
km
long
and
has
been
measured
in
three
different
surveys,
in
1966,
1986
and
2004.
For
this
line
three
different
time
intervals
have
been
studied:
1966–1986,
1986–2004
and
1966–2004.
By
comparing
the
bench-
marks
heights
measured
in
the
three
surveys,
the
total
elevation
change
which
occurred
at
the
considered
time
intervals
has
been
obtained
(Fig.
6b).
The
elevation
changes
range
between
−40
mm
and
8
mm.
Again
the
two
consecutive
elevation
changes
and
the
elevation
change
over
the
entire
time
interval
are
coherent
and
significative.
In
order
to
calculate
the
vertical
deformation
rate
in
the
time
intervals
1966–1986,
1986–2004
and
1966–2004
the
relationship
(2)
has
been
applied.
The
vertical
deformation
rates
(mm/yr),
for
each
benchmark,
were
calculated
with
respect
to
the
reference
benchmark
#11.
In
Table
3
the
relative
rates
of
vertical
defor-
mation
(mm/yr)
for
each
benchmark
are
reported.
A
schematic
geological
profile
along
the
line
(Fig.
6c)
allowed
us
to
recon-
struct
the
lithological
succession
under
each
benchmark
and
to
identify
the
possible
causes
of
vertical
deformation
(geology
from
Atzori
et
al.,
1983;
topography
from
a
2
×
2
m
grid
Lidar
flight
DTM,
http://www.pcn.minambiente.it/GN/).
5.
Data
analysis
In
this
section
we
discuss,
for
each
analyzed
leveling
line,
the
vertical
deformation
rates
obtained
by
comparison
of
repeated
Author's personal copy
6C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12
Fig.
3.
Heights
versus
elevation
changes
plotted
in
order
to
verify
the
occurrence
of
slope
dependent
errors
along
the
Line
108
(a)
along
the
Line
92
(b)
and
along
the
Line
100
(c).
leveling
measurements
and
the
possible
sources
that
caused
this
deformation.
5.1.
Line
108
In
Fig.
7a,
the
trend
of
vertical
deformation
rates
along
the
Line
108
is
shown.
This
line
has
by
far
the
greatest
elevation
change
rates,
with
maximum
change
rate
difference
of
12
mm/yr
between
the
two
extreme
benchmarks.
The
calculated
rates
are
all
signifi-
cant.
By
analyzing
in
detail
the
vertical
deformation
along
the
line,
sectors
characterized
by
different
rates
can
be
identified
(see
also
Table
1).
The
section
between
the
benchmarks
#111
and
#119
is
raised
in
comparison
to
the
reference
benchmark
(#107)
with
a
relative
and
constant
rate
of
∼3.5
mm/yr,
reaching
a
peak
of
4.0
mm/yr
in
correspondence
of
the
benchmark
#118.
Similarly,
the
section
between
the
benchmarks
#120
and
#126
shows
uplifting,
although
it
is
characterized
by
rates
lower
than
the
previous
area,
with
average
rates
of
∼2.0
mm/yr
and
with
a
peak
of
2.5
mm/yr
at
the
benchmark
#126.
These
different
values
can
be
explained
by
geological
features:
the
benchmarks
between
#120
and
#126
are
located
on
alluvial
deposits
(Fig.
4c)
and
may
be
subject
to
com-
paction
of
unconsolidated
sediments,
unlike
the
benchmarks
#111
and
#119
that
are
located
on
more
competent
lithologies
(Fig.
4c).
Alternatively,
the
difference
could
be
related
to
the
Quaternary
W-
E
trending
fault
located
between
the
benchmarks
#119
and
#120
(Fig.
4a;
Servizio
Geologico
d’Italia,
2011),
whose
elastic
strain
accu-
mulation
could
give
rise
to
a
greater
relative
uplift
(∼3.5
mm/yr)
of
the
section
between
#111
and
#119,
located
on
the
raised
block,
Author's personal copy
C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12 7
Fig.
4.
(a)
Benchmarks
of
the
Line
108,
located
in
eastern
Sicily
between
Augusta
and
Catania,
measured
in
1970
and
1991.
Crustal
seismicity
of
the
last
10
years
from
Gruppo
Analisti
Dati
Sismici,
2012.
(b)
Elevation
change
from
Augusta
to
Catania
along
the
Line
108
measured
between
1970
and
1991.
The
arrow
shows
the
reference
benchmark.
(c)
Topographic
and
lithologic
profile
along
the
Line
108.
(For
interpretation
of
the
references
to
color
in
this
figure
legend,
the
reader
is
referred
to
the
web
version
of
this
article.)
and
a
lower
relative
uplift
(∼2.0
mm/yr)
of
the
section
between
#120
and
#126,
located
on
the
downthrown
block.
The
analysis
of
crustal
seismicity
for
the
last
10
years
(Gruppo
Analisti
Dati
Sismici,
2012)
shows
that
the
many
events
are
located
near
the
fault,
espe-
cially
along
its
offshore
extension
(Fig.
3a).
It’s
worth
to
note
that
this
structure
is
mapped
as
a
normal
fault
in
the
geological
map
of
Servizio
Geologico
d’Italia
(2011)
and
previous
literature,
but
recent
geological
data
(Catalano
et
al.,
2006)
and
ground
deformation
pat-
tern
reconstructed
by
GPS
velocity
fields
(Mattia
et
al.,
2012)
clearly
define
an
area
of
prevailing
contraction
along
the
northern
rim
of
the
Hyblean
Plateau.
This
suggest
that
tectonic
inversion
could
have
recently
occurred
and
Pleistocene
normal
faulting
superseded
by
current
contractional
activity.
To
the
north,
we
observe
a
local
subsidence
along
the
area
between
the
benchmarks
#129
and
#137
(Fig.
7a;
Table
1),
with
a
maximum
peak
of
−8.6
mm/yr
in
correspondence
to
the
benchmark
#130.
Taking
into
account
that
these
benchmarks
are
located
above
the
recent
unconsolidated
silt
deposits
of
the
Simeto
river
(Fig.
4c;
Servizio
Geologico
d’Italia,
2009),
their
subsidence
can
be
related
to
strong
sediment
compaction
(Fig.
4a).
Most
Table
1
Elevation
change
rate
and
change
rate
estimated
rms
error
along
the
Line
108
for
the
1970–1991
time
span.
Locality
Line
Benchmark
name
Along
line
distance
(km)
Elevation
change
rate
1970–1991
(mm/yr)
Error
1970–1991
(mm/yr)
Melilli
108
107#
0.000
0.000
±
0.00
Augusta
108
111#
4.144
2.767
±
0.07
Melilli
108
113#
6.023
3.690
±
0.05
Melilli
108
114#
7.909
3.560
±
0.05
Melilli 108
114#
7.909
3.367
±
0.00
Augusta
108
115#
8.947
3.537
±
0.03
Augusta
108
117#
10.969
3.517
±
0.05
Augusta
108
118#
11.860
4.010
±
0.03
Augusta
108
119#
12.828
3.582
±
0.03
Augusta 108 120# 13.906
1.660
±
0.04
Augusta
108
122#
16.008
2.105
±
0.05
Augusta
108
123#
17.010
2.075
±
0.03
Carlentini
108
124#
17.718
2.100
±
0.03
Carlentini
108
125#
18.902
2.329
±
0.04
Catania
108
126#
20.224
2.793
±
0.04
Catania
108
129#
23.087
−1.540
±
0.06
Catania
108
130#
24.267
−8.646
±
0.04
Catania
108
132#
26.320
−1.558
±
0.05
Catania
108
134#
28.296
−0.781
±
0.05
Catania 108
137#
31.417
−4.796
±
0.06
Catania 108 138#
32.267
3.423
±
0.03
Catania
108
142#
37.021
3.780
±
0.07
Catania 108
143#
38.061
4.113
±
0.04
Author's personal copy
8C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12
Fig.
5.
(a)
Benchmarks
of
the
Line
92,
located
in
northeastern
Sicily,
north
of
Messina,
measured
in
1967,
1970,
1986
and
2004.
Crustal
seismicity
of
the
last
10
years
from
Gruppo
Analisti
Dati
Sismici,
2012.
(b)
Elevation
change
along
the
Line
92
measured
in
the
periods
1967–1986,
1986–2004,
1967–2004.
The
arrow
shows
the
reference
benchmark.
(c)
Topographic
and
lithologic
profile
along
the
Line
92.
(For
interpretation
of
the
references
to
color
in
this
figure
legend,
the
reader
is
referred
to
the
web
version
of
this
article.)
Table
2
Elevation
change
rate
and
change
rate
estimated
rms
error
along
the
Line
92
for
the
1967–1986,
1986–2006,
1967–2004
time
spans.
Locality
Line
Benchmark
name
Along
line
distance
(km)
Elevation
change
rate
1967–1986
(mm/yr)
Elevation
change
rate
1986–2004
(mm/yr)
Elevation
change
rate
1967–2004
(mm/yr)
Error
1967–1986
(mm/yr)
Error
1986–2004
(mm/yr)
Error
1967–2004
(mm/yr)
Messina
92
No68
0.000
0.000
0.000
0.000
±
0.00
±
0.00
±
0.00
Messina
92
002#
2.456
0.089
0.122
0.105
±
0.13
±
0.06
±
0.03
Messina
92
005#
5.625
0.153
0.222
0.186
±
0.14
±
0.07
±
0.03
Messina 92
007#
7.897
0.178
±
0.06
Messina
92
008#
8.831
−0.047
−0.022
−0.035
±
0.08
±
0.04
±
0.02
Messina
92
009#
9.949
−0.105
−0.139
−0.122
±
0.08
±
0.04
±
0.02
Messina 92 010#
11.139
−0.356
±
0.04
Messina
92
011#
12.164
−0.221
−0.472
−0.343
±
0.08
±
0.04
±
0.02
Messina 92
012#
13.173
−0.305
−0.561
−0.430
±
0.08
±
0.04
±
0.02
Messina
92
014#
15.228
−0.189
±
0.06
Messina
92
015#
16.110
−0.178
±
0.04
Messina
92
016#
17.219
−0.053
−0.039
−0.046
±
0.09
±
0.04
±
0.02
Messina
92
017#
18.123
0.150
0.075
0.114
±
0.08
±
0.04
±
0.02
Table
3
Elevation
change
rate
and
change
rate
estimated
rms
error
along
the
Line
100
for
the
1966–1986,
1986–2006,
1966–2004
time
spans.
Locality
Line
Benchmark
name
Along
line
distance
(km)
Elevation
change
rate
1966–1986
(mm/yr)
Elevation
change
rate
1986–2004
(mm/yr)
Elevation
change
rate
1966–2004
(mm/yr)
Error
1966–1986
(mm/yr)
Error
1986–2004
(mm/yr)
Error
1966–2004
(mm/yr)
RC
100
011#
0.000
0.000
0.000
0.000
±
0.00
±
0.00
±
0.00
VSG
100
014#
3.169
0.315
0.200
0.261
±
0.06
±
0.07
±
0.03
VSG
100
015#
4.307
−0.530
−0.544
−0.537
±
0.04
±
0.04
±
0.02
VSG
100
016#
5.297
−0.090
0.000
−0.047
±
0.04
±
0.04
±
0.02
VSG
100
017#
6.438
0.225
0.111
0.171
±
0.04
±
0.04
±
0.02
VSG
100
018#
7.490
0.245
0.178
0.213
±
0.04
±
0.04
±
0.02
VSG
100
020#
9.812
0.240
0.100
0.174
±
0.05
±
0.06
±
0.03
Scilla
100
022#
12.070
0.240
0.172
0.208
±
0.05
±
0.06
±
0.03
Scilla
100
023#
13.344
−0.020
−0.072
−0.045
±
0.04
±
0.04
±
0.02
Scilla
100
025#
15.457
0.365
0.306
0.337
±
0.05
±
0.06
±
0.03
Scilla
100
026#
16.607
0.245
0.144
0.197
±
0.04
±
0.04
±
0.02
Scilla
100
027#
17.699
0.265
0.167
0.218
±
0.04
±
0.04
±
0.02
Scilla
100
028#
18.758
−0.510
−0.794
−0.645
±
0.04
±
0.04
±
0.02
B
Calabra
100
031#
21.859
−0.394
±
0.07
B
Calabra 100 032#
23.069
0.265
0.111
0.192
±
0.04
±
0.04
±
0.02
B
Calabra
100
032P
23.326
0.280
0.128
0.208
±
0.02
±
0.02
±
0.01
Author's personal copy
C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12 9
Fig.
6.
(a)
Benchmarks
of
the
Line
100,
located
in
southwestern
Calabria
between
Villa
San
Giovanni
and
Bagnara
Calabra,
measured
in
1966,
1970,
1986
and
2004.
Crustal
seismicity
of
the
last
10
years
from
Gruppo
Analisti
Dati
Sismici,
2012.
(b)
Elevation
change
along
the
Line
100
measured
in
the
periods
1966–1986,
1986–2004,
1966–2004.
The
arrow
shows
the
reference
benchmark.
(c)
Topographic
and
lithologic
profile
along
the
Line
100.
(For
interpretation
of
the
references
to
color
in
this
figure
legend,
the
reader
is
referred
to
the
web
version
of
this
article.)
likely,
this
subsidence
is
the
main
cause
of
structural
failure
of
the
Primosole
Bridge
on
the
Simeto
River
which
occurred
in
2009.
(http://www.blogcatania.it/blog/2009/07/02/ponte-primosole-
chiusura-e-disagi/).
Finally,
the
northernmost
section
of
the
Line
108,
between
the
benchmarks
#138
and
#143,
shows
uplift
in
comparison
to
the
ref-
erence
benchmark
with
a
relative
rates
of
∼4.0
mm/yr
(Fig.
7a
and
Table
1).
This
deformation
may
be
related
to
the
processes
of
active
folding
(Laboume
et
al.,
1990;
Bonforte
et
al.,
2011)
at
the
front
of
the
Sicilian
chain
(Fig.
4a).
5.2.
Line
92
Fig.
7b
shows
the
trend
of
vertical
deformation
along
the
Line
92
for
the
three
analyzed
time
intervals
(see
also
Table
2).
The
rate
change
difference
between
the
two
extreme
values
is
only
0.8
mm/yr,
more
than
an
order
of
magnitude
less
than
the
previous
line
108.
The
three
time
intervals
give
coherent
change
rates
which
are
all
significant,
except
for
the
smallest
values.
During
the
first
time
interval
(1967–1986)
a
general
uplift
of
the
benchmarks
#2
and
#5,
compared
with
the
reference
benchmark
#68,
occurs.
The
maximum
rate
of
vertical
deformation
is
0.16
mm/yr
at
the
bench-
mark
#5.
Proceeding
along
the
Line
92
we
can
observe
that
the
section
between
the
benchmark
#8
and
#16
has
undergone
subsi-
dence,
with
a
maximum
peak
at
the
benchmark
#12
(−0.17
mm/yr).
Finally,
the
benchmark
#17
has
been
uplifted
in
comparison
to
the
benchmark
#68
with
a
rate
of
0.15
mm/y.
The
trend
of
vertical
deformation
during
the
second
time
inter-
val
(1986–2004)
has
been
similar
to
that
of
the
first
interval,
even
though
different
rates
were
measured
(Table
2
and
Fig.
7b).
Also
in
the
second
time
interval
the
section
between
the
benchmarks
#2
and
#5
shows
a
general
uplift
compared
with
the
reference
benchmark
#68,
with
rates
reaching
a
peak
of
0.22
mm/yr
in
corre-
spondence
of
the
benchmark
#5,
whereas
the
section
between
the
benchmark
#8
and
#16
shows
subsidence,
with
rates
reaching
a
peak
of
−0.57
mm/yr
in
correspondence
of
benchmark
#12.
These
data
confirm
the
increase
of
the
vertical
deformation
in
the
second
time
interval.
Moreover,
we
calculated
the
average
rates
of
vertical
defor-
mation
for
the
whole
time
interval
1967–2004.
Fig.
7b
shows
uplift
between
the
benchmarks
#2
and
#7
relative
to
#68,
with
a
0.19
mm/yr
maximum
rate
(see
also
Table
1),
subsidence
between
the
benchmarks
#8
and
#16,
with
−0.36
mm/yr
maximum
rate
in
correspondence
of
benchmark
#12,
and
finally
uplift
of
the
bench-
mark
#17
with
a
rate
of
0.12
mm/yr.
These
data
suggest
that
the
trend
of
the
vertical
deformation
has
remained
constant.
The
observed
vertical
deformation
along
the
Line
92
can
be
explained
by
elastic
strain
accumulation
along
the
∼N-S
oriented
normal
fault
(Fig.
5a)
located
north
of
Messina
(Gargano,
1994),
which
has
caused
uplifting
of
the
area
between
the
benchmarks
#2
and
#7
and
in
correspondence
of
the
benchmark
#17,
that
are
located
on
the
footwall
of
the
fault,
and
subsidence
of
the
area
between
the
benchmarks
#8
and
#16,
that
is
located
on
the
hanging-wall
of
the
same
structure.
5.3.
Line
100
Fig.
7c
shows
the
trend
of
the
vertical
deformation
along
the
Line
100
for
the
three
analyzed
time
intervals.
This
line
is
located
on
the
opposite
side
of
the
Messina
straits,
on
the
Italian
main-
land.
The
rate
change
difference
between
the
two
extreme
values
is
1.2
mm/yr,
an
order
of
magnitude
less
than
the
costal
line
108.
Again
the
three
time
intervals
give
coherent
change
rates
which
are
all
significant,
although
the
smallest
values
are
close
to
the
resolution
of
the
method.
The
coherence
between
the
results
cal-
culated
at
the
three
time
intervals
is
excellent,
showing
that
the
calculated
rates
are
stable
in
time.
Examining
the
first
time
interval
(1966–1986),
a
general
uplift
relative
to
the
reference
benchmark
#11
can
be
observed,
except
for
a
few
benchmarks
that
show
sig-
nificant
subsidence
(see
also
Table
3).
In
particular,
the
benchmark
#14
shows
uplift
with
a
rate
of
∼0.27
mm/yr,
the
benchmarks
#15
and
#16
show
subsidence
with
rates
reaching
a
minimum
value
of
Author's personal copy
10 C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12
Fig.
7.
Elevation
change
rate
versus
distance
along
the
Line
108
for
the
1970–1991
time
span
(a),
along
the
Line
92
for
the
1967–1986,
1986–2004,
1967–2004
time
spans
(b)
and
along
the
Line
100
for
the
1966–1986,
1986–2004,
1966–2004
time
spans
(c).
−0.53
mm/yr
in
correspondence
of
the
benchmark
#15,
the
sec-
tion
from
#17
to
#22
has
been
uplifted
with
a
constant
rate
of
∼0.24
mm/yr,
the
benchmark
#23
shows
subsidence
with
a
rate
of
−0.02
mm/yr,
the
section
from
#25
to
#27
has
been
uplifted
with
rates
up
to
0.35
mm/yr
in
correspondence
of
the
benchmark
#25.
A
significant
subsidence
is
shown
by
the
benchmarks
#28–31
that
have
been
lowered
at
a
maximum
rate
of
−0.51
mm/yr
in
corre-
spondence
of
the
benchmark
#28.
Finally,
the
benchmarks
#32
and
#32P
have
been
uplifted
with
rates
∼0.27
mm/yr.
The
trend
of
the
vertical
deformation
during
the
second
time
interval
(1986–2004)
is
similar
to
that
of
the
first
interval
even
though
a
change
in
the
rate
of
deformation
is
evident
(Table
3
and
Fig.
7c).
In
fact,
the
benchmark
#14
shows
relative
uplift
rate
of
0.09
mm/yr,
the
section
between
the
benchmarks
#15
and
#16
shows
subsidence
with
rate
similar
to
that
of
the
first
time
inter-
val
(−0.54
mm/yr),
the
section
between
the
benchmarks
#17
and
#22
has
been
uplifted
with
a
rate
reaching
a
maximum
peak
of
0.18
mm/yr
in
correspondence
with
the
benchmark
#18,
the
bench-
mark
#23
has
been
lowered
with
a
rate
of
−0.07
mm/yr,
the
section
#25–27
has
been
uplifted
with
rates
ranging
between
0.14
and
0.30
mm/yr.
The
strong
subsidence
of
the
section
#28–31
is
con-
firmed
also
during
the
1986–2004
time
interval
when
a
maximum
rate
of
−0.80
mm/yr
in
correspondence
to
the
benchmark
#28
has
been
calculated.
Finally,
the
benchmarks
#32
and
#32P
have
been
raised
with
a
lower
rate
of
∼0.10
mm/yr.
Also
for
this
line
we
calculated
the
average
rates
of
vertical
deformation
for
the
whole
time
interval
1966–2004
(Table
3
and
Fig.
7c).
During
this
period
the
benchmark
#14
shows
uplift
with
a
rate
of
0.18
mm/yr,
the
benchmarks
#15
and
#16
show
subsi-
dence
with
a
maximum
peak
of
∼−0.54
mm/yr
in
correspondence
with
the
benchmark
#15,
the
section
from
#17
to
#22
shows
an
uplift
with
maximum
values
of
0.21
mm/yr
in
correspondence
to
the
benchmark
#18,
the
benchmark
#23
documents
a
subsidence
characterized
by
a
rate
of
∼−0.05
mm/yr,
the
section
#25–27
shows
uplift
with
rates
ranging
between
0.2
and
0.34
mm/yr.
Finally,
the
benchmark
#
28
shows
−0.64
mm/yr
average
rate
of
subsidence,
whereas
the
benchmarks
#32
and
#32P
document
∼0.2
mm/yr
average
rate
of
uplift.
We
observe
that
the
trend
of
vertical
defor-
mation
along
the
Line
100
has
remained
constant
during
the
past
40
years,
being
characterized
by
alternations
of
uplift
and
subsidence
relative
to
the
reference
benchmark
#11.
One
possible
cause
of
the
vertical
deformation
along
the
Line
100
is
the
occurrence
of
elastic
strain
accumulation
along
active
tectonic
structures
intersecting
the
line
in
south-western
Calabria.
By
comparing
data
obtained
from
high
precision
leveling
with
the
trace
of
the
SW-NE
striking
Scilla
normal
fault
(Ferranti
et
al.,
2007,
2008)
along
the
coast
between
the
towns
of
Bagnara
Calabria
and
Villa
San
Giovanni
(Fig.
6a),
we
can
observe
subsidence
and
uplift
of
the
benchmarks
located
on
the
hanging-wall
and
on
footwall
of
the
fault,
respectively.
In
particular,
an
excellent
correlation
between
the
instrumental
data
and
the
geometry
of
the
fault
is
suggested
by
the
benchmarks
#14,
#17,
#18,
#20,
#22,
#25,
#26,
#27,
#32
and
#32P,
which
indicate
uplift
at
the
footwall
of
the
fault,
and
by
the
benchmarks
#15,
#16,
#23
and
#28,
which
document
subsidence
at
the
hanging-wall
of
the
same
structure
(Figs.
6a
and
7c).
The
only
incompatibility
between
instrumental
and
geological
data
has
been
observed
in
correspondence
of
the
benchmark
#31,
which
indicates
a
subsidence
although
located
on
the
footwall
of
the
fault.
This
can
explained
by
the
site
of
the
cornerstone
#31,
that
it
is
located
above
unconsolidated
and
saturated
alluvial
deposits
(Fig.
6c)
subject
to
compaction
processes.
The
recent
activity
of
the
Scilla
normal
fault
is
confirmed
by
macro-seismic
and
palaeo-seismological
data
(Jacques
et
al.,
2001;
Ferranti
et
al.,
2007,
2008)
and
by
the
crustal
seismicity
of
the
last
10
years
(Fig.
6a)
(Gruppo
Analisti
Dati
Sismici,
2012;
see
also
Scarfì
et
al.,
2009;
Neri
et
al.,
2012).
6.
Discussion
and
conclusions
The
analysis
of
instrumental
data
obtained
by
repeated
mea-
surements
of
high
precision
leveling
during
the
last
40
years
allowed
us
to
estimate
very
recent
vertical
movements
in
some
sectors
of
eastern
Sicily
and
southern
Calabria
(e.g.
the
Messina
Straits).
We
can
summarize
the
results
as
follows:
•Line
108
(Fig.
7a),
measured
in
two
different
campaigns
(1970
and
1991)
in
south-eastern
Sicily,
shows
a
general
uplift
proceeding
from
south
to
north
with
the
exception
of
the
area
between
the
Author's personal copy
C.R.
Spampinato
et
al.
/
Journal
of
Geodynamics
66 (2013) 1–
12 11
benchmarks
#129
and
#137
which
results
in
subsidence
due
to
compaction
of
alluvial
deposits
of
the
Simeto
River.
Moreover,
major
uplift
of
the
section
between
the
benchmarks
#111
and
#119
with
respect
to
the
section
between
the
benchmarks
#120
and
#126
can
be
related
to
elastic
strain
accumulation
along
the
W-E
striking
fault
separating
the
Catania
Plain
from
the
Hyblean
Plateau
(Fig.
4a).
However,
the
diffused
low-energy
seismicity
shows
that
elastic
strain
accumulation
can
be
released
also
by
small
ruptures
along
this
structure.
•Line
92
(Fig.
7b),
measured
in
four
distinct
surveys
(1967,
1970,
1986
and
2004)
shows
a
constant
trend
of
vertical
deformation.
For
the
three
analyzed
time
periods
(1967–1986,
1986–2004
and
1967–2004),
an
uplifting
sector
(benchmarks
#2,
#5,
#7
and
#17)
can
be
distinguished
from
a
subsiding
area
(benchmarks
between
#8
and
#16;
Fig.
7b),
as
a
possible
consequence
of
elastic
strain
accumulation
along
a
N-S
striking
fault
occurring
north
of
the
town
of
Messina
(Fig.
5a).
•Line
100
(Fig.
7c),
measured
in
4
different
campaigns
(1966,
1970,
1986
and
2004)
shows
a
constant
rate
of
vertical
deformation.
For
the
three
analyzed
time
periods
(1966–1986,
1986–2004
and
1966–2004)
uplifting
sectors
(benchmarks
14,
#17,
#18,
#20,
#22,
#25,
#26,
#27,
#32
and
#32P)
can
be
distinguished
from
subsiding
ones
(benchmarks
#15,
#16,
#23
and
#28).
This
ver-
tical
deformation
can
be
related
to
elastic
strain
accumulation
along
the
NW-SE
striking
Scilla
normal
fault
(Fig.
6a).
It
is
inter-
esting
to
note
that
Ferranti
et
al.
(2008)
estimated
a
co-seismic
throw
rate
of
∼1
mm/yr
along
this
structure
during
the
last
3.5
ka,
as
effect
of
two
large
pre-historic
earthquakes.
This
value
is
very
close
to
that
estimated
here
by
the
difference
between
uplifting
and
subsiding
benchmarks,
indicating
that
over
the
last
40
yr
the
strain
accumulation
is
comparable
to
that
coseismically
released
in
the
past.
Although
the
processing
of
the
different
time
series
high
pre-
cision
leveling
has
allowed
us
to
estimate
only
the
relative
rates
due
to
the
lack
of
an
absolute
reference
point,
their
extreme
accu-
racy,
together
with
the
large
extension
of
networks,
make
this
type
of
measurement
fundamental
for
the
estimate
of
recent
vertical
deformation.
In
addition,
correlating
instrumental
and
geological
data
makes
it
possible
to
identify
active
tectonic
structures
respon-
sible
for
vertical
deformation.
Taking
into
account
that
it
is
mostly
related
to
elastic
strain
accumulation
along
crustal
discontinuities
(King
et
al.,
1988;
Stein
et
al.,
1988;
Yeats
et
al.,
1997;
Scholz,
2002),
this
kind
of
analysis
can
provide
important
clues
for
the
reconstruc-
tion
of
the
seismic
cycle
of
seismogenic
faults.
This
proposition
has
important
engineering
implications
for
the
planning
of
the
∼3
km
long
single-span
bridge
on
the
Messina
Straits.
We
show
that
the
active
normal
faults,
identified
from
geolog-
ical
mapping,
have
an
imprint
on
the
present
vertical
movements
roughly
between
0.5
and
1
mm/yr.
The
vertical
movements
due
to
compaction
of
fluvial
sediments
are
much
higher,
and
reach
the
value
of
up
to
13
mm/yr
relative
to
the
nearby
consolidated
rock.
Acknowledgements
We
thank
L.
Ferranti
ant
an
anonymous
reviewer
for
their
com-
ments
that
helped
to
clarify
some
aspects
of
the
work
and
M.
Mattia
for
helpful
discussions.
The
research
was
funded
by
grants
from
University
of
Catania
(responsible
C.
Monaco)
and
University
of
Tri-
este
(responsible
C.
Braitenberg).The
leveling
data
were
provided
by
the
Italian
Istituto
Geografico
Militare
(IGM)
only
for
scientific
purposes.
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