Bousquet and Gueremy (1968) and Bousquet (1973)
These authors recognise, map and refer to Quaternary the Pollino Fault and three 
NNW-trending fault scarps located between Castrovillari and Frascineto, 
successively named Castrovillari Fault scarps (Cinti et al., 1995). 

Moretti and Chiodo (1992)
They analyse the stratigraphy and tectonic setting of the Upper-Pleistocene 
lacustrine marls and medium to coarse grained fan delta sediments of the 
Frascineto-Castrovillari basin and point out that the nearly N-trending fault 
scarps that cut the lacustrine surface near the village of Frascineto show 
recent activity as prevalently normal faults. Soft sediment deformations, 
liquefactions and fluidification structures are interpreted as evidence of the 
occurrence of large seismic events in the area.

Ferreli et al. (1994)
These investigators identify previous unmapped fault scarps cutting quaternary 
fan deposits, along a 18 km long section of the Pollino Fault between the 
village of Civita and the locality of Masseria Marzano. On the basis of 
trenching analyses they recognise evidence for two events of surface faulting, 
the most recent one of Holocene age. They also highlight the presence of late 
Pleistocene and Holocene activity along the N-trending scarps of the 
Castrovillari Fault and of the Monte Moschereto fault, supposing they are 
secondary structures slipping as a consequence of the primary Pollino structure.

Cinti et al. (1995a, b)
They study and map the Castrovillari Fault scarps located south to 
the Pollino Range between the village of Castrovillari and Frascineto. This 
structure intersect the surface by forming three NNW-trending and W-facing 
scarps that can traced for a length of about 10 km. These scarps cut fluvial and 
lacustrine deposits of Pleistocene and Holocene age. On the basis of 
paleoseismological and geomorphological observations and analyses of models of 
deformation pattern, they infer that the Castrovillari Fault is the main 
seismogenic source present in the Pollino area. They point out that part of the 
western section of the Pollino Fault slipped at the same time with the 
Castrovillari Fault, at least during the most recent event. In this 
interpretation the Pollino Fault would represent a barrier to a further northern 
propagation of the Castrovillari fault.

Ferreli et al. (1995)
On the basis of radiocarbon dating show that the two events they recognised in 
the exploratory trenches in the central section of the Pollino Fault west of its 
junction with the Castrovillari Fault, are of historical age. They also suppose 
that these events occurred a 18 km long section of the Pollino Fault, between 
Masseria Marzano and Civita.

Vittori et al. (1995)
They recognise at least two and possibly three surface faulting events in the 
Masseria Quercia Marina trench site and by means of radiocarbon dating of 
charcoal samples they give an age of about 1550 years B.P. for event B. 
They point out that the recent movement is prevalently dip slip with no or 
minor horizontal components, with slip rates of 0.1 to 0.5 mm/yr.

Cinti et al. (1997)
By means of exploratory trenching they study the paleoseismicity of the 
Castrovillari Fault; they recognise at least four paleo-events of surface 
faulting during the past 30 Kyr. The most recent event occurred between 380 B.C. 
and 1200 A.D., probably nearly 760 A.D.. On the basis of their observations and 
dating, they propose a preliminary estimate of the main fault parameters: 
vertical slip rate of 0.2-0.5 mm/yr and minimum recurrence interval of 1170 
year.

Cinti et al. (2001)
Further trenching provides new constraints on the age of the most recent event 
between 530 and 900 A.D. or 530 AND 1100 A.D. They also provide further 
geomorphic support to the hypothesis that the Castrovillari fault is the main 
seismogenic source in the area.
