Biasini (1966)
He identifies two prominent fault scarps at Piano di Pezza and in 
locality "Tra le Fosse" (Campo Porcaro), that are part of a main 
dislocation line. These scarps are interpreted as the surface 
evidence of an active normal fault that produced as much as 9 m of 
post-Wurm displacement. 

Giraudi (1988)
On the basis of aerial photo analyses, he suggests that the fault at 
Campo Porcaro has an horizontal component of movement that is 
substantially larger than the vertical component. He estimates: (1) 
7-8 m of vertical and 12-15 m of left lateral displacement during 
the past 7,000 years, and (2) 17 m of vertical and 65-70 m of left 
lateral displacement during the past 18,000 years.

Giraudi (1989)
He describes in detail the late Quaternary stratigraphy of the region 
and estimates horizontal and vertical displacements of glacial and 
Holocene sediments. He suggests that two strong seismic events ("seismic 
crises") are responsible for these displacements that occurred between 
18,000 and 15,000 years B.P. and between 7,000 and 4,700 years B.P., 
respectively.

Cinti et al. (1992a)
They reconstruct in detail the topography of a section of the fault 
scarp at Piano di Pezza and show that the fault movement at this 
location is prevalently normal.

Cinti et al. (1992b)
By means of trenching investigations at Piano di Pezza, they provide 
a preliminary age for the most recent surface faulting event on this 
fault, which is constrained to be between 1019 and 1349 A.D. They also 
point out that this event is not reported in any of the current catalogues of 
Italian seismicity.

D'Addezio et al. (1995)
On the basis of considerations on the history of local settlements 
they provide better constraints for the age of the most recent 
earthquake described by Cinti et al. (1992b) that should have occurred 
before 1400 and possibly before 1300 A.D.

D'Addezio et al. (1996)
Based on microtopographic and trenching investigations, they definitely 
reject the hypothesis that the Campo Porcaro section of the Ovindoli-Pezza 
Fault is characterised by prevalent horizontal movement.

Pantosti et al. (1996)
Using geological, geomorphic and paleoseismological observations, they 
characterise the seismic behaviour of the Ovindoli-Pezza Fault; they 
estimate an average recurrence time ranging between 1,000 and 
3,300 years, and a vertical slip rate of about 1 mm/yr. They also conclude 
that, at a regional scale, the Ovindoli-Pezza Fault trace can be simplified and 
seen as a NW-striking, SW-dipping fault with a geometry similar to that of 
the Fucino seismogenic source. They calculate a NE-SW oriented 
extension rate using both slip rates obtained from trenching and long-term 
displacement rates from geomorphic observations. Their estimated 
extension rates from trenching and from displaced geomorphic features fall 
in the range 0.3-0.5 mm/y and 0.4-1.1 mm/y, respectively. 

Galadini (1999)
On the basis of an integrated data-set, he describes 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 ceased their activity, 
while other NW- to NNW-trending faults began to be characterised by 
left-lateral to oblique sinistral slip. The N160-striking portion of the 
Ovindoli-Pezza Fault would be one of these. At the same time, pure normal 
movement is observed along N125- to EW-trending faults as along the Piani 
di Pezza Fault. According to Galadini the horizontal component of motion 
decreases from south to north, and the Ovindoli-Pezza Fault is characterised 
by 1:1 ratio. 

Piccardi et al. (1999)
The investigators interpret the recent tectonic evolution of the area 
as leaded by a deep-seated left-lateral shear zone: they calculate an 
extension oriented N2010E, with a rate ranging between 1 and 3 mm/yr 
in the Fucino area, that suggests a left-lateral component of motion between 
Adria and Tyrrhenia along the central Apennines. In their interpretation the 
NNW-striking structures, like the Ovindoli-Pezza fault are characterised by 
left-lateral oblique component of motion, and are the shallow expression of 
the deep seated shear zone.

Cinti et al. (2001)
They test the hypothesis that the Ocre fault is part of the Ovindoli-
Pezza source by developing detailed geomorphic and paleoseismologic 
investigations of the Ocre range. Paleoseismological trenching shows 
evidence for of the occurrence of at least three displacement events 
occurred between 1000 A.D. and 5035 B.C. The most recent event recognised 
on the Ocre fault section occurred between 1000 A.D. and 1705 B.C. Because 
the age of this displacement event is consistent with the age of the 
penultimate event found on the Ovindoli-Pezza section the investigators 
suppose that these events may be synchronous and support the hypothesis 
of a single seismogenic source containing the Ovindoli-Pezza, Cefalone, and 
Ocre fault sections.
