Oddone (1915)
Based on a survey performed immediately after the occurrence of the 1915 
earthquake, this investigator describes and maps in detail the formation of 
several fractures in the plain and of a "voragine" running along the south-
western side of Monte Serrone and downdropping the south-western side; he 
interprets these features as due to differential compaction between the 
sediments of the old lake and the slope detritus and the bedrock.

Gasparini et al. (1985)
These workers provide a fault plane solution of the January 13, 1915 
earthquake by analysing polarities of the first motions of P-wave arrivals 
recorded at 23 seismic stations all over the word. The best solution given by 
the seismic inversion is a N298 striking, 39 dipping plane, characterised by 
almost pure left lateral slip.

Basili and Valensise (1986)
These investigators relocate the 1915 earthquake epicentre on the basis of the 
arrival time of the first motion in several Italian and European seismic 
stations; they calculate the fault plane solution of the event, giving a left 
lateral faulting mechanism with a little dip component on a N138 striking, 
68 dipping best fitting plane.

Giraudi (1986)
Based on the analysis of aerial photos, this investigator analyses several 
faults cutting the sediments of the old Fucino lake and the Holocene-Upper 
Pleistocene terraces surrounding it. In the middle of the plain the faults are 
highlighted by linear contacts of soils characterised by different lithologies 
and moisture contents; closer to the basin margin they correspond to fault 
scarps displacing the terraces. According to the author these faults are of 
Holocene age and may have moved in historical time, although only few of 
them correspond to the scarps generated by the 1915 earthquake.

Bonasia et al. (1986)
These investigators use the geodetic levelling dataset formed by a pre-event 
survey performed in 1862 and by a post-event survey, in order to analyse 
static surface displacement associated with the January 13, 1915 earthquake, 
and give the fault plane geometry with a direct modelling. The authors 
provide as best result of their modelling a N112E striking, 70SW dipping, 18 
km- long plane, located about 7 km SW of the Serrone Fault, in contrast with 
geological evidence of surface faulting along this fault.

Serva et al. (1986) and Blumetti et al. (1987)
Through a reinterpretation of the work of Oddone, achieved by interviewing 
several eye-witness of the 1915 earthquake, and based on a geomorphological 
survey carried out in the north-eastern area of the Fucino plain, these workers 
reconstruct and describe in detail the geometry of  the fault scarps related to 
that event. According to them the surface faulting consisted of two sub-
parallel about 10 km long fractures formed between the villages of Sperone 
and S. Benedetto dei Marsi and between the south-western side of Mt. 
Parasano and the village of Cerchio, downthrowing the south-western side. 
The authors also describe the stratigraphic succession exposed in a gravel 
quarry present in the San Veneziano area (south-eastern sector of the Plain) 
that shows the evidence of at least three surface faulting events in the last 
13,000 years, post the deposition of the gravel.

Giraudi (1989)
Through a geomorphological study of the Fucino Plain and of correlations 
between ages of rock collapses in caves and ages of morphological features, 
this paper supplies a chronology of the inception of several fault scarps, 
present in the eastern side of the plain and near the town of Avezzano, and 
of the earthquakes related to them. In fact on the basis of morphological 
considerations he considers each scarp related to a single earthquake; he 
recognises and dates four events, three of pre-historic age (between 
18-20,000 and 13-14,000 years B.P.; between 5,500 and 5,000 years B.P.; nearly 
3,100 years B.P.) and one of Late Roman or Middle Ages age (484 or 508 
A.D.?), related to a fault scarp cutting a Roman age channel.

Ward and Valensise (1989) and Valensise(1989)
These investigators model static surface displacement related to the 1915 
earthquake using the geodetic dataset formed by the pre-event and the 
post-event surveys, and model the geometry of the related fault using 
uniform and variable slip planar dislocation models. These 
analyses reveal a two lobed slip pattern separated by a central zone of low 
moment release, in agreement with geomorphological observations of 
landform features and of the fault scarps related to that event, with a N135 
striking, 63 dipping, 24 km long and 15 km wide best fitting fault plane. 
According to the authors the present shape of the Fucino basin could 
represent the long term result of repeated events that occurred on the 1915 
Fault and on the Tre Monti Fault.

Quattrocchi et al. (1990)
This paper describes and measures natural degassation phenomena (mostly 
methane) observed at various locations along the southern side of the Plain. 
The phenomena are interpreted as due to the degassation of small natural 
reservoirs due to the especially dry season and to the subsequent increase in 
rock premeability. However, their locations align along the Trasacco Fault, 
providing indirect evidence for its activity.

Brunamonte et al. (1991)
These investigators describe three exploratory trenches opened across one of 
the two fault scarps related to the 1915 earthquake, near the village of San 
Benedetto dei Marsi, and on the basis of the analyses of the stratigraphic 
sequence and of radiocarbon dating of samples recognise two 
paleoearthquakes referred to VI-IX century a.D. and X-XIV century a.D. 
respectively.According to them these events may have been of the same 
magnitude as the 1915 earthquake.

Galadini and Messina (1994)
This paper describes the geological and tectonic evolution of the Fucino 
Basin, by means of stratigraphic, geomorphological and structural analyses. 
According to these authors the ENE-trending Tre Monti fault zone, that 
borders the northern margin of the Fucino plain, was responsible for the first 
phase of opening of the basin during the Pliocene; later in the Upper Pliocene 
and Quaternary times the evolution of the basin was mostly influenced by 
the NW-trending faults of the eastern margin of the plain (San Benedetto dei 
Marsi-Gioia dei Marsi and Marsicana Highway faults), whose activity 
continued up to the present.

Landini (1994)
She estimates a long term-slip rate for the Fucino fault of about 1.7 mm/y 
on the basis of the uplifted "Pescina terrace", located on the footwall of the fault. Modeling of this presumably 700 ka feature suggests that 1,200 m of fault slip are needed to uplift it and tilt it from horizontal to slighlty NE-dipping.

Galadini et al. (1995).
These investigators recognise in the stratigraphic succession exposed at three 
distinct sites several surface faulting events: two trenches digged for pipeline 
supplies to the south of the village of Cerchio, and cutting the 1915 
earthquake fault scarp, showed the evidence of four palaeoearhquakes, one of 
which occurred before 19100 yr B.P., two of them after this date and the last 
after 2800 yr B.P.; hand boring performed across the 1915 scarp near the village 
of Venere gave the evidence of an Upper Middle Ages age event; at last in an 
open quarry near the village of Casali d'Aschi they recognize four events 
with age ranging between 2,800 yr B.P. to the Middle Ages.

Galadini and Galli (1996)
By means of trenching at the intersection between a Roman-age channel and 
the Trasacco Fault, these investigators supply evidence for the occurrence of a 
surface faulting earthquake that displaced the channel excavated for drainage 
purpose by the Romans during the I-II century a.D.; on the basis of geological, 
historical and archaeological data they demonstrate that this event occured 
between VI and IX century a.D., and that it can be likely related to the 508 a.D. 
earthquake that was responsible for severe damages to the Colosseum in 
Rome or in second hand to the 618 a.D. earthquake. They also hypothyze that 
this event could be considered as a twin of the 1915 earthquake, as 
paleoseismological trenching analyses in the eastern side of the Fucino Plain 
near the village of San Benedetto dei Marsi showed the presence of a surface 
faulting event of high Medieval age characterized by displacements with 
similar offsets along the same fault scarps of the 1915 event, giving then a 
first estimation of recurrence interval of about 1300-1400 years, for this 
seismogenic fault.

Galadini et al. (1996)
On the basis of paleoseismological analyses conducted at four sites along the 
Trasacco Fault, these investigators describe seven surface faulting earthquakes 
and give the age of the last three occurred before the 1915 event (6000-5000 
years B.P.; 3400-3200 years B.P.; while the third may be related to the 508 a.D. 
earthquake); they propose a recurrence time  of about 1,500-2,000 years for events 
similar to the 1915 earthquake, and calculate the slip rate, which varies between 
0.36 mm/yr and 0.15 mm/yr for the past 7,000 years moving northward along the 
Trasacco Fault.

Michetti et al. (1996)
This paper describes the results of trenching performed near the village of 
San Benedetto dei Marsi on one of the coseismic scarps related to the 1915 
earthquake. They recognise at least two surface faulting events besides the 
1915 one, almost characterized by similar coseismic displacement, and 
constrain their age with archaeogical materials and by radiocarbon dating of 
soil samples; according to them event B occurred between 550 and 885 a.D., 
and very likely it can be related to the 801 a.D. earthquake; they suggest the 
best estimate age range of event A is between the end of X century a.D. and 
1349 a.D., then relating it to an earthquake of medieval age not recorded in 
the historical catalog. On the basis of the coseismic displacement registered on 
the fault scarp, they also hypothize that these two events were of the same 
magnitude of the 1915 earthquake.

Amoruso et al. (1998)
These investigators present a nonlinear inversion to determine the source 
parameters of the 13 Jan. 1915 earthquake, utilizing as input data both vertical 
displacement, deriving from the geodetic dataset formed by the pre-event 
(1862) and the post-event (1917) surveys, and seismic data (P wave first 
motions). The best fitting model geometry obtained with the assumption of 
uniform slip on a planar fault in a homogeneous elastic half-space, is a N143 
striking, 55 dipping, 35 km-long fault plane, whose surface projection match 
with the serrone Fault. The authors point out that the right lateral 
component of slip used in the modeling is in agreement with structural, 
geological and geomorphological observations made on active faults found in 
the Fucino region.

Galadini (1999).
This paper uses a vast integrated dataset to describe the Quaternary kinematic 
evolution of the Fucino plain and of other tectonic basins of the central 
Apennines. He shows that starting from the beginning of the Middle 
Pleistocene some NW-trending normal faults interrupted their activity, 
while others NW- to NNW-trending faults began to be characterised by 
left-lateral to oblique sinistral slip (N160-striking portion of the Ovindoli-Pezza 
Fault and Upper Sangro Fault Zone); in the same time pure normal movements 
are observed along N125 to EW-trending faults (Velino, Marsicana Highway 
and San Benedetto-Gioia faults). According to his interpretation the change 
in fault kinematics may have been caused by the evolution of the northern 
Apennines arc characterized by progressive eastward migration of the 
compressive front followed by the extension, while the southeastern margin 
remained fixed.

Galadini and Galli (1999)
This paper present a summary of all the palaeoseismological data available 
for the Fucino Plain. The Fucino seismogenic source is intepreted to be 
formed by a primary fault system, consisting in the Marsicana Highway Fault 
and in the San benedetto-Gioia Fault, bordering the eastern side of the basin, 
with associated secondary faults, Trasacco Fault and Luco dei Marsi Fault, 
found in the middle of the plain and close to the western side of the margin. 
Following this interpretation large magnitude earthquakes generated by the 
primary fault system would induce passive slip on the secondary faults. 
Previous workers by means of paleosesimological analysis in different sites of 
the Fucino plain identified ten surface faulting events in the last 33,000 years, 
seven of which occured during the Holocene. Dating of geological and 
archeological features allowed a chronology and a calculation of the average 
recurrence interval for surface faulting earthquakes, that resulted ranging 
between 1,400 and 2,600 years. On the basis of the observed offset vertical slip 
rate were computed for individual fault branches, ranging between 0.24 and 
0.5 mm/yr for the primary fault system, and between 0.1 and 0.27 mm/yr for 
the secondary faults. Galadini and Galli on the basis of the slip rate data 
collected calculate a minimum value for the extension rate across the Fucino 
basin ranging between 0.6 and 1 mm/yr in a NE-SW direction.

Piccardi et al. (1999)
These investigators carry out a detailed geomorphic and structural study of 
the faults found around the Fucino basin and give an estimation of their 
vertical slip rates.The authors consider the fault sytem responsible for present 
day active deformation in the Fucino plain to be formed by four NW-
trending parallel faults (Serrone, Parasano, Muricci and Ventrino faults) 
found along the northeastern margin of the basin, and splying with a right-
stepping horsetail geometry from the NNW-trending oblique left-lateral 
Sangro-Giovenco Fault found more to the east; to the north these faults are 
truncated by the ENE-trending oblique right-lateral Tre Monti Fault. 
Following geomorphic analysis of the heights of the fault scarps, and 
assuming that the measured offset postdate the end of periglacial abrasion 
(144 kyr BP), the authors provide estimate of vertical slip rates, maximum 
expected magnitudes and average recurrence times for each individual fault 
branch; the ranges of the long term vertical slip rates calculated for the 
Serrone, Parasano and Ventrino faults result to be between 0.5 and 1.4, 0.5 and 
1.0, and 0.3 and 1.1 mm/yr respectively. On the basis of measurements of the 
most recent slip indicators found on the bedrock scarplets and of 
geomorphological considerations the authors show that the NW-trending 
faults are characterized by a more or less component of right lateral oblique 
slip, and hypothesize that they accomodate extension in a N20E direction; 
the calculated extension rate across the Fucino area, considering average fault 
geometry and throw rates, would be between 1 and 3 mm/yr.
