Gars (1983)
He studies the recent tectonics of the Gargano promontory and highlights an 
episode of important uplift accompanied by some extension lasting up to the 
deposition of the Lower Pleistocene "tuffs" (sandstone). According to this paper 
a N20 compressional event follows as suggested also by reverse faulting contact 
110-striking and 47NE-dipping of the Mesozoic bedrock over the "tuffs". In 
this interpretation, at present the compression appears to have rotated to 145-
170.

Suhadolc et al. (1983)
They present a statistical investigation of the seismicity of the broad Gargano 
region and recognise the main seismogenic alignments in the area. They also 
conclude that there is a different seismic behaviour in the eastern and western 
part of the Promontory and that there is a relation, in terms of temporal 
behaviour, between the Gargano and Irpinia region. 

Meloni and Molin (1985)
They study the macroseismoc field of the 1875 and 1889 earthquakes and highlight 
a peculiar large extension of the VIII and VII MCS intensity areas. They attempt 
a correlation of this peculiarity with the geologic and tectonic setting of the 
area. Location of both events appears to be close to the western portion of the 
Mattinata fault.

Funiciello et al. (1988) and Funiciello et al. (1991) 
These papers present a reconstruction of the tectonic evolution of the Gargano 
promontory since the Paleogene. The authors recognise a first extensional phase 
on faults N40-50W that dissected a wide anticline forming the bulk of the 
promontory; a successive phase associated to the activation of the Mattinata 
fault as a left-lateral strike slip structure, and finally an extensional 
phase on faults E-W, NW-SE and NE-SW. They do not find evidence for present 
activity on the Mattinata fault but for a fault south of it.

Ortolani and Pagliuca (1988)
On the basis of meso- and macro-structural analysis they describe the tectonic 
setting and the history of deformation of the Gargano promontory. They conclude 
that the present setting of the promontory is related to a sequence of different 
tectonic phases: the Eocene-Oligocene "dinaric" phases, and the Miocene and 
Plio-Quaternary Apenninic phases. They also propose a reconsideration of the 
Gargano seismicity under this light.

Caldara and Palmentola (1991)
They describe the marine terraces that indent the promontory slopes highlighting 
that the Gargano promontory experienced important uplift since Mio-Pliocene.

Argnani et al. (1993)
Through the interpretation of seismic reflection profiles they highlight the 
main structures existing offshore the Gargano promontory. The easterly 
prolongation of the Mattinata fault surely appears in the offshore data although 
it does not have any morphological evidence at the sea bottom. This interpreted 
by the authors as the consequence of the fact that the main activity on this 
structure occurred in Eocene times and was completed by Early Pliocene. At 
present no important horizontal or vertical slip can be recognised. On the 
contrary, to the north, the Tremiti Islands zone seems to show Quaternary 
activity. However, the authors point out that both zones are preferential 
location for seismicity.

Favali et al. (1993a) and Favali et al. (1993b)
These papers interpret the Gargano area as an active deformational belt 
controlled by two main systems: the dextral Tremiti Islands system to the north, 
and the sinistral Mattinata system to the south. These systems are the 
preferential location for instrumental seismicity and recent seismic swarms. No 
attempt in locating the source of the 1627 earthquake is presented.

Doglioni et al. (1994) and Doglioni et al. (1996)
By analyzing the Apenninic foreland study the tectonic setting of the Gargano 
promontory they conclude that it results to be controlled by two dextral 
tectonic lines: the Tremiti Islands and Mattinata lines. According to these 
authors the Gargano promontory is located at the northern edge of the southern 
part of the foreland that, in contrast with the central Adriatic ended with 
subsidence after Pliocene-Early Pleistocene and is now experiencing important 
uplift. No discussion about seismicity is presented.

Guerricchio and Pierri (1998 and references therein of same authors) 
These papers define the main fault systems of the Gargano area on the basis of 
Landsat imagery analysis, aerial photos, and subsurface data. These systems have 
a broad spectrum of strikes NW-SE, ENE-WSW, and E-W as well as various 
kinematics. They also analyse the seismicity of the broad Gargano area and point 
out that there is potential for M7 earthquakes such as the 1627 but, that the 
several events located along the Mattinata fault show only small to moderate 
magnitude and no M>6 event is expected along this feature.

Piccardi (1998)
The author highlights the existence of several faults that appear to be active 
in the Gargano area.  Among them the Mattinata fault is the most impressive and 
shows an E-W trend. He proposes a subdivision of this large structure in three 
sections, from east to west they are Monte Sant' Angelo, San Giovanni Rotondo, 
and San Marco in Lamis. This structure is interpreted as a main dextral strike 
slip fault, with sizeable vertical component, that is evidence for crustal 
compression. Present seismicity is mainly of small magnitude and its 
distribution does not outline any clear trend. The author provides the source 
parameters for the Monte Sant'Angelo section.

Salvi et al. (1999)
This paper presents the results of a multidisciplinary study aimed to the 
implementation of a geochemical GIS. The main tectonic features in the Gargano 
area are identified in the Mattinata fault, considered left-lateral, the 
Candelaro and Rignano faults. Geochemical anomalies of the ground-waters are 
found along the Mattinata fault, the Candelaro river, and on a WSW lineament 
south of the Lesina lake. 

Catalogo Parametrico dei Terremoti Italiani (1999)
The 1875 San Marco in Lamis earthquake is reanalysed in this Catalogue and a new 
equivalent magnitude of 6.2 is attributed from the previously 5.4. 
