323,163 research outputs found
The growth of the Chianti Ridge: progressive unconformities and depositional sequences in the S. Barbara Basin (Upper Valdarno, Italy)
No full textThe Chianti Ridge, elongated in a NW-SE direction, separates the Upper Valdarno from the Siena Basins. It is made of Macigno and
Scaglia Toscana Fms. belonging to the Tuscan Nappe that underlies the Ligurian Units. Inside the Upper Valdarno basin three main
synthems have been identified, separated by major unconformities; from the bottom: 1. Castelnuovo synthem, subdivided into
Spedalino and Meleto subsynthems, 2. Montevarchi synthem and 3. Bucine synthem. The Spedalino subsynthem, that unconformably
lies over the pre-Pliocene bedrock, is made up of thin and laterally discontinuous coarse gravels. The Meleto subsynthem, commonly
referred to a lacustrine environment, is made of alluvial plain lithofacies, including channel, crevasse splay and swamp depositional
systems where a Taxodium forest developed and peat accumulated. Close to the western margin of the basin these subsynthems are
tilted up to 60°. The Montevarchi synthem, mainly made of sands and gravels accumulated inside a wide braidplain, and lies
unconformably over the previous units. This synthem is tilted eastward up to 20°. Finally, the Bucine synthem lies unconformably over
the previuos synthems generating a fluvial terrace of the Arno River. The two lower units date back to the Early Pliocene. In fact the
Meleto clays contain mammal remains that can be found in the Triversa Faunal Unit (Early Villafranchian, late Early - Middle Pliocene)
as well as in the Ruscinian (Early Pliocene). They are also negatively magnetized and could correspond to the Gilbert Chron.
Palaeomagnetic investigations and the presence of aeolian sediments in the Montevarchi synthem and cold pollen flora allowed its
attribution to the Middle and Late Pliocene. The relationships between the different synthems and the dominant unconformities coupled
with thermochronological data recently obtained in the Apennine ridge to the east (BALESTRIERI et al., 2003) allow us to establish
that the Chianti Ridge, after a major planation, became the eastern edge of a moderate relief (Spedalino subsynthem) that was later
transformed into a wide alluvial plain (Meleto subsynthem). Updoming tilted the previous units before the modelling of a second major
unconformity that preceed the deposition of the Montevarchi synthem. It is possible that during this period the Valdarno was still connected
to the Siena Basin to the west. A third major unconformity followed finally separating the two basins. These deformations
occurred almost at sea level. During the Early and Middle Pliocene, the Apennine Ridge to the east did not exist and the Upper
Valdarno represented the western part of the peri-Adriatic Basin. The deepening of the drainage network is due to the generalised
uplift that in the nearby areas started during the Early Pleistocene. Finally the creation of the present-day Apennine watershed was not
gradual but very rapid in the geological time scale and started mostly during the Early Pleistocene
PRELIMINARY BIOSTRATIGRAPHIC DATA FROM CASTELNUOVO GARFAGNANA BASIN (LUCCA, TUSCANY, ITALY).
No full textThe Castelnuovo Garfagnana basin, which is investigated since 1800s for mining of lignite
and quarrying of clay, is filled by Villafranchian continental deposits for long time interpreted
as fluvio-lacustrine sequences (De Stefani 1889, D'Amato Avanzi & Puccinelli, 1988; Masini,
1936; Calistri, 1974; Puccinelli, 1987). A recent survey by Landi et al. (2002) provides a more
detailed paleoenvironmental reconstruction, mapping four different lithostratigraphic Units. The
lithostratigraphic Unit l is referred to a cohesive sediment anabranching river system developed
in moist climatic conditions. This lithostratigrafic Unit, which represents the more ancient fluvial
system recorded, mainly consists of spread fine clayey, silty and sandy deposits, characterized
by accumulation in si tu of lignite (Overbank architectural elements ), and, subordinately, of
conglomeratic deposits (Channel belt architectural elements). The lithostratigraphic Unit 2, 3
and 5 are chiefly composed of conglomeratic deposits (Channel belt architectural elements),
respectively related to: (i) gravel bed-load alluvial system (lithostratigraphic Unit 2), (ii) debris
flow dominated fan (lithostratigraphic Unit 3), and (iii) braided fluvial fan (lithostratigraphic
Unit 5).
The age of these deposits represents a matter of debate. Several previous studies suggested
a generalized Villafranchian age (De Stefani, 1887, Zaccagna, 1932; Masini, 1933). Because of
the occurrence of a diversified mammal assemblage (Anancus arvernensis, Lynx cf. issiodorensis,
Sus cf. minor, Tapirus sp.) (De Stefani, 1887, 1889) in deposits related to the basal portion
of lithostratigrafic Unit l of Landi et al. (2002), Azzaroli (1977) and Antiga (1988) proposed
a Lower Villafranchian age (correlable with the Triversa Faunal Unit). In the middle portion
of lithostratigraphic Unit l instead, the presence of charophyte gyrogonites, which belong
to the species Nitellopsis cf. megarensis, and fresh-water molluscs (Theodoxus cf. groyanus,
Prososthenia paulae and Prososthenia sp.) is indicative of a Middle Villafranchian age, corresponding
to the Late Pliocene (Souliè-Marsche, 1979; Gliozzi et al., 1997; Esu & Girotti, 2001).
The age of the successive lithostratigraphic Units is unclear. However, some ostracod val ves
assigned to the species Cyprideis torosa have been collected in the basal portion of the lithostratigraphic
Unit 2. According to Gliozzi et al. (1997), this species is commonly found in Pleistocene
sediments with a stratigraphic range, which extends from Late Villafranchian to Aurelian.
The different biostratigraphical setting of the lithostratigraphic Units l and 2 is consistent with
the hypothesized presence of a disconformity between these two Units, as inferred by Landi et
al. (2002)
Sedimentologic and paleontologic obsrvations on the Castelnuovo Garfagnana Villafranchian basin (Lucca, Tuscany, Italy)
No full textThe Castelnuovo Garfagnana Basin is located along the intramontane valley of the Serchio
River. This basin extends approximately for 15 Km in length and it is separated from the contiguous
Barga Basin by a structural high, currently known as "Soglia di Monte Perpoli" (Puccinelli,
1987). From a regional point of view, the two basins represent a tectonic extensional
depression delimited southwest by the Apuan Alps and northeast by the Apennines.
The geologica! investigation of the Castelnuovo Garfagnana Basin began in the 1800s
because of the presence of abundant lignite deposits. The sedimentary succession of this basin
consists of continental deposits, mainly of Villafranchian age, for long time related to a generi c
fluvio-lacustrine environment (see e. g., D'Amato Avanzi & Puccinelli, 1988; Puccinelli, 1987).
A recent geologica! and sedimentological survey of this area (Landi et al., 2002) argues about
the presence of four different litostratigraphic Units, which were deposited by two river systems
and some tributaries that flowed respectively, longitudinally an d laterally to the axis of the basin.
The litostratigraphic Unit l , bere discussed in detail from both a sedimentological and a paleontological
point of view, represents the earliest fluvial system recorded irt this area, which is
mainly characterized by often fossiliferous, fine-grairted, deposits. By contrast, the other
litostratigraphic Units prevalently consist of sterile conglomeriltes.
The sedimentary succession of the litostratigraphic Unit l lies in disconformity on metamorphic
and non-metamorphic Falda Toscana and Ligurian Units. The thickness of the entire
succession, which measures about 200m., was estimated on both seismic and geologica! evidences
(Cancelli et al., 2002).
The succession described by Landi et al. (2002) mainly consists of fine-grained deposits,
related to overbank elements (swamp, pond, levee and muddy-flood plain, coded respectively as
SW, PO, L and M in Landi et al., 2002), with intercalations of conglomerates and sand lithosomes.
The latter are irtterpreted as channel belt elements (simple channel fill and heterolithic
bar, coded respectively as CH and HB in Landi et al., 2002). The overbank elements L, M, SW
and PO are represented by silty, sandy or muddy deposits. M and L deposits, mainly constituted
by silty, clayey and sandy lithofacies, show some intercalations of hydromorphic paleosoils containing
remains of land molluscs (e.g., Helix sp., Pomatias elegans, Discus rotundatus). Freshwater
fossi! taxa, such as charophytes (Chara vulgaris, Lychnothamnus barbatus), ostracods
(Candona neglecta, Candona sp., Ilyocypris gibba), molluscs (Bithynia sp., Prososthenia paulae, Theodoxus cf. groyanus), and fishes (Barbus cf. plebejus, ? Chondrostoma sp., Leuciscus
souffia, Rutilus aff. rubilio, Scardinius erythrophthalmus), are also commonly found in
these sediments. From a sedimentological point of view, these elements are clearly indicative of
a floodplain depositional environment (Landi et al., 2002) and this interpretation is consistent
with the paleontological assemblage.
SW elements, which were deposited in swamp environments, are characterized by the widespread
presence of both Glyptostrobus trunk remains, which lack of any evidence of transport,
and leaves. PO deposits are represented by a rhythmic altemation of laminated clays and silts,
containing abundant fossi! remains and sideritic glaebulae (Landi et al., 2002). A more detailed
paleontological study was carried out in these deposits. The fossi! assemblage consists of charophyte
gyrogonites (Chara vulgaris, Lychnothamnus barbatus, Nitellopsis cf. megarensis), plant
remains, freshwater ostracods (Candona spp., Ilyocypris gibba) , gastropods (Melanoides curvicosta,
Theodoxus cf. groyanus), and fish remains (Scardinius erythrophthalmus). The paleontological
characters confirm that the PO elements were deposited in smalllakes (Lychnothamnus
barbatus and Nitellopsis cf. megarensis; Bathia et al. , 1998) and temporary ponds (Chara vulgaris;
Soulié-Marsche, 1993), characterized by anoxic conditions at bottom (Flores, 1981) as
supposed in Landi et al. (2002). The occurrence of abundant fish remains (bones and teeth) is
consistent with the information derived from facies analysis and charophyte gyrogonites. As discussed
by Smith et al. (1988) delicate fish bone remains in floodplain environments are common
only in fine-grained deposits related to swamps, ponds or smalllakes
Caratteri geomorfologici della fascia costiera compresa tra la foce del fiume Albegna, la Laguna di Orbetello ed Ansedonia
No full textLa fascia costiera compresa tra la foce del Fiume Albegna e il promontorio di Ansedonia è una costa mista la cui genesi è stata dominata prevalentemente da processi erosivi in corrispondenza del promontorio del M. Argentario e di Ansedonia e da processi deposizionali nei cordoni litorali limitrofi. La crescita dei cordoni litorali è fortemente condizionata dagli apporti fluviali dell’Albegna a nord e del Fiora a sud. L’analisi geomorfologica ha permesso di individuare le varie tappe dell’evoluzione costiera e della genesi della laguna verificatesi durante l’Olocene. Sono stati individuati numerosi paleoalvei dell’Albegna che hanno creato degli apparati deltizi sia prima della genesi dei cordoni che successivamente. La massima ingressione olocenica ha generato una scarpata di erosione che ha interessato, terrazzandoli, depositi di conoide alluvionale, fluviali, detritici ed eolici deposti durante l’ultima fase fredda pleistocenica. Terrazzi minori associati alla divagazione laterale di meandri ad ampio raggio di curvatura e paleoalvei caratterizzano il bordo settentrionale della pianura dell’Albegna
Geoarcheologia dell’insediamento musteriano di "Grotta Reali" ed evoluzione delle sorgenti del Volturno (Molise)
No full textNew sedimentoogical data from the Villafranchian deposits of Castelnuovo Garfagnana and Barga basins (Lucca, Tuscany, Italy)
No full textThe Castelnuovo Garfagnana and Barga basins are
located about 25 km north of Lucca along the
intramontane valley of the Serchio river. They are
about 5 Km wide, 15 and IO Km respectively long
and are separated by a structural high, known in
literature as "Soglia di Monte Perpoli" (Puccinelli,
1987). These basins constitute a tectonical
extensional depression, elongated in a NW-SE
direction, delimited southwest by the Alpi Apuane
and northeast by the Apennines. The geologica!
history of the Castelnuovo Garfagnana and Barga
basins, as the other depressions formed along the
Tyrrhenian margin of the Apennine chain, is related
to the Tyrrhenian rifting, active since late Tortonian,
and the counter-clockwise migration of the chainforedeep-
foreland system (Patacca et al., 1990). The
two basins, studied since 1800 for mining of lignite
and quarrying of clay, are filled with a remarkable
thickness of continental deposits, mainly of
Villafranchian age, generically interpreted in
literature as fluvio-lacustrine (Masini, 1936; Calistri,
1974). This study aims at offering a more detailed
reconstruction of the depositional history of these
deposits. A geologica! survey 1/ 10.000 scale,
together with sedimentological and compositional
analysis and paleontological data, allow to locate
five informai litostratigraphic units, whose
geometrica! relationships are shown in Fig. l. Within
each unit, a various number of lithofacies can be
seen (Miall, 1996 and, Sanchez-Moya et al., 1996
lithofacies code are used) and their association
allows to define some architectural elements (Miall,
1996). Their features and their geometrica!
relationships give rise to a more detailed and
complex reconstruction of the depositional history of
the Vi llafranchian deposits. Sixteen conglomeratic,
heterolithic, sandy and silty-clay lithofacies were
distinguished and grouped in nine architectural
elements belonging to channel belt elements and
overbank elements. The channel belt elements
consist of conglomeratic deposits (isolated channels
!C, grave! bar GB, debris flow deposit DF),
heterolithic and sandy elements (heterolithic bar HB
and sandy bar SB), while swamp (SP), pond (PO),
levee (L) and muddy-floodplain (M) constitute the
fine-grained overbank elements. On this basis four
alluvial depositional systems can be recognized. The
basai fluvial system, corresponding to
lithostratigraphic Uni t l , li es in disconformity o n the
substratum made by the metamorphic and nonmetamorphic
"Falda Toscana" units and subordinate
"Ligurian" units. !t is composed mainly of fine-
54
grained deposits, related to overbank elements with
intercalation of conglomeratic and sandy lithosomes
(Channel belt elements). Within overbank elements
SP deposits are characterized by widespread
presence of lignite (C lithofacies) and subordinate
intercalation of clays (Fm lithofacies). Tree trunks in
life-wise position have been observed. Vegetai
remains of G/yptostrobus sp., are consistent with
humid-subtropical climatic conditions. PO element is
characterized by rhythmical alternations of clay and
silt (Fh, Fsm and Fm lithofacies) containing freshwater
taxa like ostracodes (Candona spp. 1/yocypris
gibba), gastropods (Me/anoides curvicosta,
Prososthenia paulae Theodoxus sp. Laminifera
vi/lajranchiana), teeth of fish (Tinca sp., Leuciscus
cepha/us), together with charophytes oogonia and
leaves. L and M elements consist respectively of
rhythmical alternations of fine sand, silt, clay (Sh,
Fsm, Fm lithofacies) and clay and silty-clay (Fm,
Fsm lithofacies). Widespread presence of
hydromorphic paleosols (P lithofacies) containing
land taxa (e.g. Helix sp. , Pomatias e/egans, Discus
rotundatus) is observed mainly in M element.
Channel belt elements consist of isolated channels
(IC) and heterolithic bar (HB). IC element shows a
ribbon geometry and frequently "ailes d' etalement"
(sensu Friend et al. , 1979). Width-depth ratio is
consistent with stable channels. They are composed
of polygenic, grain-supported conglomerate (Gp, Gt
and Gcm lithofacies), frequently organized in fining
upward trend. HB element shows a plane-convex
upward geometry and consists of alternations
between sand and grave! (Ep, Et, St, Sp lithofacies)
organized in fining upward trend. They represent
bars migration within the channel. Compositional
data and paleocurrent analysis (northwest to
southeast direction) are consistent with a single
longitudinal (sensu Miall, 1996) fluvial course
flowing through the two basins. The whole acquired
data is consistent with the characteristic of cohesive
sediment anabranching river system, organo-clastic
sub-type (sensu Nanson & Knighton, 1996). The
second alluvial system recognized corresponds to
lithostratigraphic Uni t 2 (Fig. l). Unlike the
underlying system, Unit 2 is mainly composed of
conglomerates (channel belt elements), while finegrained
deposits (overbank elements) are
subordinate. GB and SB elements constitute channel
belt elements. GB element is made up of openwork
and matrix-filled conglomerates (Gp and Gt
lithofacies), frequently organized in fining upward
trend. Reactivation surfaces are frequently observed. SB element consists of medium to coarse-grained
sand (Sp and St lithofacies) sometimes containing
clay soft clasts. GB and SB associations are
interpreted to represent bars migration within the
channel. L and M elements constitute the overbank
elements. They are respectively characterized by fine
to medium-grained sand (Sh and Sr lithofacies) and
by drapes of clay (Fm lithofacies), while immature
paleosols (P lithofacies) are common in M element.
L and M deposits show strong affinities with the
actual overbank deposits of Serchio river. Deposits
belonging to this unit are related to a gravel bed load
braided system (sensu Sanchez-Moya et al., 1996).
Compositional and paleocurrent analysis point out
more or less the same longitudinal fluvial course,
flowing through the two basins, observed for the
underlying cohesive anabranching river system
organo-clastic sub-type. Along the Castelnuovo
Garfagnana and Barga margins, spatially limited
conglomeratic lithosome, showing latero-vertical
relationships with Unit l and 2 (Fig. l) are mapped.
Lithostratigraphic Unit 3 crops out along the
Apennine margin of the two basins. !t consists of
channel belt elements of very coarse massive
monogenic conglomerate (Gcm and Gmm
lithofacies), exclusively derived from the
surroundings "Macigno" F ormation. The same
textural characteristics were observed in the
litostratigraphic Unit 4 (Fig. l) cropping out in a
small area of the southwest margin of the Barga
basin. Besides "Macigno" clasts, the conglomerate is
also composed of deriving "Falda Toscana" and
Methamorphic units clasts. The close proximity of
source area and textural features are consistent with a
debris flow dominated fan (sensu Stanistreet & Mc
Carthy, 1993) developed transversally to the basi n' s
axis. The lithostratigraphic Unit 5 crops out in the
southwest margin of the Castelnuovo Garfagnana
basin and consists of channel belt elements.
Lithofacies Gp, Gt e Sm, (polygenic, clast supported
conglomerate and medium-coarse grained sand)
representing the composition of surrounding area are
associated in GB element. Paleocurrent analysis
shows a radiai pattem. This unit is interpreted as a
braided fluvial fan alluvial system (sensu Stanistreet
& McCarthy, 1993) developed transversally to the
basin 's axis. The whole acquired data lead to
delineate the depositional history of villafranchian
deposits cropping out in the Castelnuovo Garfagnana
and Barga basins. The results of this study can be
summarized in two principal points: i) onset, in a
humid sub-tropical climate phase, of a first alluvial
system, flowing through the two basins and related
to a cohesive sediment anabranching river (sub-type
organo-clastic) characterized by a prevalent finegrained
overbank organic-rich sedimentation. At the
same time coalescent debris flow dominated fan,
mainly derived from Apennines margin, forms
transversally to the basins axis. ii) Development of a
gravel bed load braided alluvial system,
characterized by prevalent gravelly channel belt
deposits, flowing through the two basins. The
erosive contact between this system and the
underlying one, is an abrupt facies change inferring a
possible disconformity surface. At the same time
debris flow dominated fans derived from the
Apennines margin continue to develop. Although the
proposed reconstruction involves the necessity of a
disconformity surface also within these deposits, the
spatially limited outcrops and the frequently
weathering do not permit to evaluate this hypothesis.
During this depositional phase a braided fluvial fan
derived from the Apuan Alps develops transversally
in the Castelnuovo Garfagnana basin. This
palaeoenvironment reconstruction implies that
Monte Perpoli high plays a different role compared
to that proposed by other authors. In our
interpretation, according to the sedimentological and
statistica! compositional data (Sodini M. et al.,
2002), this area acted as a sedimentary by-pass since
the opening (Lower Villafranchian) of the
Castelnuovo Garfagnana and Barga basins. This
interpretation is consistent with most recent data
about Alpi Ar uane uplift times (Molli G., 2001)
Insufficienza renale acuta e o subacuta richiedente dialisi in corso di malattia ateroembolica renale: impatto sulla sopravvivenza del paziente e del rene.
No full textThe Villafranchian deposits of the Castelnuovo Garfagnana and Barga Basins (Lucca, Tuscany, Italy): facies analysis and paleoenviromental reconstruction
No full textA facies analysis of the Villafranchian continental
deposits outcropping in the Castelnuovo Garfagnana and Barga
basins allow the reconstruction of their paleoenvironmental
evolution that differs significantly from the traditional fluvio-
lacustrine interpretation. We identify, at different stratigraphic
positions, two main river systems and some tributaries
which flowed longitudinally and laterally to the axis of
the two basins respectively, the latter fed both by the Apuan
and Apennine margins. The mapped deposits were subdivided
in five lithostratigraphic units (U1-5). Lying in disconformity
on the substratum U1 corresponds to a cohesive sediment
anabranching river (sub-type organo-clastic) developed
longitudinally to the axis of the two basins in a humid subtropical
climate phase. It is characterized by abundant fine
organic-rich deposits and lignite accumulation (overbank elements)
and by conglomeratic facies (channel-belt elements).
An abrupt facies change characterizes the contact between U1
and overlying U2 that is constituted by prevalent conglomeratic
deposits (channel-belt elements) and interpreted as a
gravel bed-load braided river. U3, U4 and U5 correspond to
coalescent fan systems developing transversally to the axis of
the two basins. U3 and U4 were interpreted as debris flow
dominated fans exclusively, (U3), or prevalently, (U4), constituted
by «Macigno» clasts while U5 corresponds to a braided
fluvial fan mainly characterized by a high variety of metamorphic
clasts. Their influence, as transversal tributaries of
the main longitudinal river systems, results both from compositional
statistical analyses of conglomeratic deposits and
from survey evidences. This paleoenvironmental reconstruction
implies that Monte Perpoli high («Soglia di Monte Perpoli
» Auctt.) acted as a sedimentary by-pass since the opening
of the Castelnuovo Garfagnana and Barga basins
La sequenza archeologica di Barbiano – Caserma dei vigili del fuoco (Bolzano) : evidenze di sistemazioni dei versanti durante il neolitico
No full textIl sito di Barbiano è stato occupato in varie fasi dalla Preistoria all’Età Romana Le prime evidenze insediative risalgono all’inizio del Neolitico medio, circa 7000 anni BP. L’occupazione venne preceduta dalla creazione di una ampia piattaforma, un terrazzo, realizzato asportando i depositi fluvioglaciali e la sovrastante copertura pedologica. La piattaforma venne completata con il riporto su tutta la superficie di alcuni decimetri di sabbia. Si tratta di una delle più antiche evidenze di significative modificazioni antropiche del paesaggio in area alpina. Questi importanti lavori suggeriscono inoltre che l’ampia area insediativa fosse abitata per la maggior parte dell’anno. L’insediamento marca dunque la transizione dalle più antiche attività agricole basate sulla pratica dello "slash and burn" a quelle stanziali. I livelli neolitici vennero coperti da sedimenti alluvionali e colluviali deposti come conseguenza dell’attivazione di processi di degradazione dei versanti innescati dalla deforestazione. Durante l’Età Romana il torrente locale era delimitato da argini artificiali ed una serie di strutture murarie vennero edificate per delimitare e proteggere aree insediative che però si sviluppano al di fuori dell’area scavata. I sedimenti grossolani all’interno del canale suggeriscono che limitati processi erosivi ancora interessavano il versante. I livelli romani sono stati successivamente sepolti da una sottile coltre colluviale che suggeriscono come i versanti sovrastanti, oggigiorno largamente terrazzati, non sono più stati interessati da processi erosivi che sono invece noti in altre aree della regione.The archaeological succession of Barbiano-Firehouse (Bozen): evidence of slope terracing during the Neolithic
Barbiano archaeological site was occupied at various stages from the Prehistory to the Roman era. The earliest occupation of the area, seems to have occurred at the beginning of the Middle Neolithic, around 7 ka bP. It was preceded by the excavation of a large almost flat platform, a terrace, realised with the stripping of fluvioglacial deposits and the overlying soil cover. The platform was later covered with a few decimetre-thick layer of sand. This is one of the earliest evidence of important anthropogenic topographic and landscape modification in the Alps. These important works suggest that the large occupation surface was probably settled for most of the year following the transition from the nomadic agriculture and the "slash and burn" practices usually associated with the Neolithic . The Neolithic settlement was lately buried under colluvial and alluvial sediments that indicate slope degradation processes most probably triggered by deforestation. In Roman Times the local stream was delimited by artificial levee and a series of walls were built to delimitate and protect larger structures that extended beyond the excavated area. The coarse sediments that fill the channel bear witness that limited erosional processes still affected on the slope. The Roman structures were buried under shallow colluvial deposits suggesting that the overlying slope, nowadays largely terraced, did not experienced anymore erosive processes that are known to have occurred in nearby areas
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