Brancaccio et al. (1981)
They analyse the geomorphology of the Baronia, a NW-trending 15 km-long Cenozoic 
ridge bounded to the SE and to the SW by the Ufita River and to the NE by the 
Fiumarella Creek. They find that the SW side of the Baronia shows two erosional 
surfaces about 10 km-long, one at the top of the relief and the other between 
500 and 600 m a.s.l. The lower surface is interpreted as a glacis; it is 
connected to the actual thalweg of the Ufita River by a NW-SE, 12 km-long 
alignment of 100-150 m-high faceted spurs interpreted by the authors as evidence 
for anactive normal fault with the west-side down. The authors infer Holocene 
and historical seismic activity of this fault on the basis of:
1) the well preserved fault slope in contrast to the high erodible 
deposits; 2) some small fluvial terraces observed in the valleys of 
the north tributaries of the Ufita river; 3) the north tributaries 
abrupt angle junctions; 4) some small scarps at the base of the 
fault slope; 5) the location and the NW trend of the mesoseismal 
areas of the 1688, 1702, and 1732 A.D. earthquakes.

Ciaranfi et al., (1983)
The Neotectonic Map of Southern Italy Interval IV-V (time-interval 0.7 Myr-0.018 
Myr and 0.018 Myr-today) shows a NE-dipping, active normal fault, located along 
the upper Ufita River Valley and a SW-dipping, likely active normal fault, 
located along the lower Ufita River Valley even though not specifically defined 
as potential seismogenic sources.

Pantosti and Valensise (1988; 1989)
Within their fault segmentation model for the Southern Apennines named "Southern 
Apennines Fault", obtained by merging macroseismic observations and 
interpretation of field evidences, they propose the Ufita Valley Fault as a NW-
striking, NE-dipping 30 km-long blind seismogenic source. They support their 
hypothesis observing that 1) the Ufita River drainage network has a regular 
pattern across the damage areas whereas it has a dendritic form in the 
surrounding areas;2) the Ufita River tributaries are in erosion while the Ufita 
Riveris aggrading; 3) the main damaged area of the 1732 earthquake is included 
between Apice to the north and Guardia dei Lombardi to the south for a distance 
of 30 km, has a NW-strike, and an asymmetrical distribution suggesting a NE 
dipping fault plane; 4) similarity with Irpinia Fault. 

Alessio et al. (1993)
On the basis of macroseismic and instrumental investigations identified four 
seismogenic areas marked by a characteristic seismic behaviour: the Southern 
Abruzzo area, the Molise area, the Beneventano area, and the Campania-
Lucania area. The Beneventano seismogenic area includes the 1125, 1688, 1702, 
1732 A.D. earthquakes. From analysis of the recent and current seismic activity 
in this zone, a swarm-type activity with sequences of comparable magnitude 
concentrated in time and space is observed.

Basso et al. (1996a; b) and Basso et al. (1997)
Re-analyzing in detail the geomorphology of the Ufita Valley area (from 
Grottaminarda up to Vallata) confirm the presence of two erosional surfaces and 
of the NW-SE fault first described by Brancaccio et al. (1981). They also 
describe six fluvial terraces and a set of NE-SW striking faults.The highest 
erosional surface is at 800-1100 m a.s.l.; the lowest surface is at 550-700 m 
a.s.l., it occurs only along the north side of the Ufita River, 150 m above its 
present-day thalweg, and is interpreted as glacis. In agreement with Brancaccio 
et al. (1981) the NW-SE striking 12 km-long alignment of 100-150 m-high faceted 
spurs connecting the lower surface to the present thalweg of the Ufita River
is interpreted as evidence for an active SW-dipping normal fault called Ufita 
River Fault. The faceted spurs have an average dip of 15 to the SW. On the 
basis of stratigraphic correlation a Late Pliocene-Early Pleistocene and 
an Early Pleistocene-Middle Pleistocene age are assigned respectively to the 
highest and the lowest surfaces. They refer to Middle Pleistocene the main 
reactivation of the Ufita River Fault and, in agreement with Brancaccio et al. 
(1981), suggest the fault was active during Holocene and historical time. They 
observe that Ufita River Fault is antithetic to the Southern Apennines Fault 
proposed by Valensise and Pantosti (1988).The six fluvial terraces they 
describe are located between 3 and 120 m above the present-day thalweg. The I-II 
order terraces are located only on the faceted spurs between 50 and 100 m while 
the III-VI order terraces occur along both sides of the river. The I-II order 
terraces are partly offset by the Ufita River Fault. The NE-SW faults they 
describe are: 1) the Parolise-Grottaminarda line, active between Middle Pliocene 
and Quaternary with a normal movement; 2) the left-lateral strike-slip Bagnoli 
Irpino-Torrente Calaggio line, active between the Pliocene and Middle 
Pleistocene; 3) the Ufita Valley Normal Fault, that is a late Pleistocene 
reactivation of the Parolise-Grottaminarda line.
