Anais da Academia Brasileira de Ciências
ISSN: 0001-3765
aabc@abc.org.br
Academia Brasileira de Ciências
Brasil
Hayakawa, Ericson H.; Rossetti, Dilce F.
Late quaternary dynamics in the Madeira river basin, southern Amazonia (Brazil), as
revealed by paleomorphological analysis
Anais da Academia Brasileira de Ciências, vol. 87, núm. 1, marzo, 2015, pp. 29-49
Academia Brasileira de Ciências
Rio de Janeiro, Brasil
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Anais da Academia Brasileira de Ciências (2015) 87(1): 29- 9
(Annals of the Brazilian Academy of Sciences)
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Instit to Nacional de Pes isas s aciais / INP Observa o da erra ivis o de Sensoriamento emoto (OB / S )
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Ancient draina e systems are bein increasin ly doc mented in the Amazon basin and their characterization
is crucial for reconstructing uvial evolution in this area. Fluvial morphologies, including elongate belts,
are well reserved alon the adeira iver. i ital levation odel from the Sh ttle adar o o ra hy
ission favored the detection of these feat res even where they are covered by dense rainforest. hese
aleomor holo ies are attrib ted to the shiftin osition of ast trib taries of the adeira iver thro h
av lsions. hese radial aleodraina e networ s rod ced fan-sha ed mor holo ies that resemble
distrib tary me afans. istin ishin av lsive trib tary systems from distrib tary me afans in the
sedimentary record is challen in . adeira s aleodraina e reveals the s er osition of trib tary channels
formed by m lti le av lsions within a iven time eriod rather than downstream bif rcation of coe istin
channels. Channel av lsion in this Amazonian area d rin the late
aternary is related to tectonics d e
to feat res as: (i) strai ht lineaments coincident with fa lt directions (ii) northeastward tiltin of the
terrain with aternary strata and (iii) several draina e anomalies incl din fre ent ortho onal draina e
in ections. These characteristics altogether lead to propose that the radial paleodrainage present at the
adeira iver mar in res lts from s ccessive av lsions of trib tary channels over time d e to tectonics.
‡
Œ
: aleochannels Amazon Basin
adeira river remote sensin
ƒ‹ ‚‰•€‹ ‚ƒ
ar e tro ical river systems are increasin ly
bein investi ated (see n mero s references in
Latrubesse et al. 2005) chie y because of the
interest in nderstandin their ori in and evol tion
as well to establish models that hel reco nize
ancient analo s. Of all modern me ariver systems
the Amazon is the lar est one with a draina e
Correspondence to: Dilce de Fátima Rossetti
-mail: rossetti dsr.in e.br
climate tectonics.
area of 6 000 (103 m2) mean ann al dischar e
of 209 000 m3 s-1 and sediment load of 167 tons
m-2 year-1. N mero s st dies have em hasized the
hydrolo ical sedimentolo ical eochemical and
morphological characteristics of this uvial system
(e.g., Gibbs 1967, Sioli 1984, Franzinelli and
I re a 2002
ertes and
nne 2007 atr besse
2008). oreover several st dies have contrib ted
to describe ancient draina e systems in Amazonia
with em hasis on aleoclimate (e. . atr besse
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
and amonell 199
ller et al. 1995 atr besse
2002) tectonics (Sternber 1950 Iriondo and
Suguio 1981, Souza Filho et al. 1999, Latrubesse
and ancy 2000 Costa et al. 2001) and sea-level
chan es (Irion 198
ital and Statte er 2000)
d rin the late aternary.
Further efforts are still needed in order to
create a lar er database before a consens s can
be reached concernin the nderstandin of the
main factors that have controlled the ori in and
evol tion of Amazonian rivers. he reconstr ction
of aleomor holo ies still reserved on the
Amazonian landsca e can contrib te to reach this
oal. he ri ht mar in of the adeira iver one of
the main Amazon trib taries is an area of s ecial
interest for this investi ation beca se it contains
an ab ndance of mor holo ies related to ancient
draina e networ s ( a ro et al. 1978 atr besse
2002). he latter a thor based on the analysis of
andsat and radar ima es considered this ancient
draina e as art of a me afan de ositional system
develo ed in the Amazonian landsca e as a res lt
of dry climates d rin the ast lacial a im m.
The de nition of a megafan, as used in this
wor has been debated in the literat re and
alternative terms such as uvial fan or terminal fan
have also been proposed (see Nichols and Fisher
2007 North and arwic 2007 for a review).
In eneral descri tions of ancient me afans are
rare with a few analo s bein the
na of the
Ebro Basin in Spain (Friend 1989, Stanistreet and
McCarthy 1993, Nichols and Fisher 2007), the
evonian de osits of the
nster Basin in Ireland
(Williams 2000), and the Wood Bay Formation of
the Bay of Spitsbergen in England (Friend and
oody-St art 1972). Additionally the e istence
of several either contin o s or discontin o s
me afans has been ro osed alon the Andean
Chain as a res lt of mo ntain lift in the northern
ran es d rin the iocene (e. . il inson et al.
2010 see also eier et al. 2005 artley et al.
2010 eissmann et al. 2010).
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
he wides read reco nition of me afans in the
eolo ical record has been recl ded by the lac of
criteria to distin ish me afan lithofacies from ty ical
uvial lithofacies. The characterization of megafans
is challen in even in modern settin s. his is mainly
due to their large dimensions that make it dif cult to
obtain a com lete view of the entire system as well
as the de cient understanding of their sedimentary
rocesses. As a conse ence descri tions of ancient
and modern me afans are still incom lete with the
ma ority of the information bein related to me afans
of the O avan o in So th Africa (Stanistreet and
cCarthy 1993
mbricht et al. 2001) the osi
anda and ista of the an ean-Brahma tra
re ion (Sinha et al. 2005 Cha raborty et al. 2010) and
the a ari in Brazil (Assine 2005).
e to the lar e dimensions of me afans remote
sensin has been the main tool sed to characterize
them in modern and
aternary settin s. i ital
levation odel (
) derived from the Sh ttle
adar o o ra hy ission (S
) re resent a
new o ort nity for im rovin the record of aleomor holo ies in areas of dense forest s ch as the
Amazonian rainforest (e. . ossetti 2010). Previo s
blications have demonstrated the sef lness of this
tool for the detection of many aleodraina e systems in
the region (Almeida Filho and Miranda 2007, Rossetti
and aleriano 2007 Silva et al. 2007 antelli et al.
2009 aya awa et al. 2010 Bertani et al. 2013).
he wor
resented here combines
S
and o tical ima es to im rove the detection
of aleodraina e networ s at the ri ht mar in of the
adeira iver. hese new data are inval able to: (i)
reconstr ct channel dynamics over time (ii) reassess
their otential relation with me afan systems and
(iii) discuss their signi cance for analyzing the
main factors that controlled channel mi ration and
abandonment in this Amazonian lowland.
he st dy area is located on the ri ht mar in of
the adeira iver and encom asses the Ari an -
A
A
NA
Madeira inter uve and both margins of the Jiparaná
River (Fig. 1A). This area is located approximately
300 m so th to so thwest of the city of ana s
IA
NA ICS IN A A ONIA
in the State of Amazonas and the second area is
located 150 m northeastward of the city of Porto
elho in the State of ondonia.
ocation of the st dy area and main rivers in Central Amazonia.
e etation ma of the st dy area (rectan le)
and its s rro ndin s. he elon ated areas of ioneer formations corres ond to some of the aleomor holo ies em hasized in this
wor . ( e etation classes accordin to a ro et al. 1978).
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
he climate is tro ical with a short dry
season (Am in Köppen`s classi cation), mean
ann al tem erat re of 28 C and mean ann al
reci itation of 2 500 to 3 000 mm year-1. he
rainy season be ins in October with reci itation
peaking between January and February and a dry
eriod between ne and A
st. he to o ra hy
is at, with SRTM elevation between 150 and
60 m. he re ion is dominated by latosols
and secondarily odzols ( a ro et al. 1978)
and ve etation cover is mostly dense lowland
ombrophilous forest, including non- ooded
upland and seasonally ooded ar ea/ allery
forests with narrow strin s of ioneer ( rassy and
bushy) vegetation (Fig. 1B).
from Ca
. OSS
I
eolo ically the st dy area lies within the
so thwestern and so theastern arts of the Amazonas
and Solim es sedimentary basins res ectively
(Fig. 2). The former, an intracratonic rift due to Early
Paleozoic intra late e tension covers to 515 000
0 000 m2 is a
m2. he latter encom assin
foreland basin also formed by intra late e tension
b t combined with deformation d rin the rise of
the Andean Chain in the Cretaceo s and Cenozoic
(A ol ceno Neto and s bone 1988). hese basins
se arated by the P r s Arch are bo nded by the
iana Shield to the north and the Central Brazil
Shield to the so th. he r
and I itos Arches
se arate the Amazonas and Solim es basins from the
ara
raben System and Acre Basin res ectively.
Limits of the Amazonas and Solimões Basins, where the study area (inside box) is located (modi ed
to and Silva 1990).
he Amazonas and Solim es basins were
develo ed over i neo s metamor hic and volcanosedimentary Precambrian basement roc s ( ei eira
et al. 1989). e osition in these basins was initiated
in the Proterozoic and contin ed in the Paleozoic. he
sedimentary ll of the Amazonas Basin consists of
several eolo ical nits formed d rin the Ordovicianarly evonian
evonian- arly Carbonifero s
and
iddle Carbonifero s-Permian. he main
hase of sediment acc m lation in the Solim es
An Acad Bras Cienc (2015) 87 (1)
Basin occ rred between the mid evonian and the
Permian. Sediment de osition was reactivated d rin
the Cretaceo s and Cenozoic. Cretaceo s de osits
re resented in both basins consist of the Alter do
Chão Formation, which includes red sandstone,
m dstone con lomerate and intraformational breccia
related to uvial, lacustrine (Daemon 1975), and
deltaic de ositional systems ( ossetti and Netto
2006). he Cenozoic de osits which occ r mainly
in the Solim es Basin incl de the iocene Solim es
A
A
NA
and the Plio-Pleistocene Içá Formations (Cunha et
al. 199 ) as well as several nnamed Pleistoceneolocene de osits ( ossetti et al. 2005). he
Solimões Formation (Miocene) consists of shales
and sandstones formed in lac strine to transitional
marine settin s (e. . onsch 1998 esslin h et al.
2001). Plio-Pleistocene to olocene de osits occ y
a lar e ortion of the western Amazonas Basin and
are represented by the Içá Formation, as well as other
unnamed Quaternary successions. The Içá Formation
is characterized by non-fossilifero s sandstones
IA
NA ICS IN A A ONIA
s bar oses and to a lesser e tent m dstones
formed mainly in braided river systems ( ossetti et
al. 2005). he
aternary de osits nconformable
with nderlyin nits are artic larly well develoed west of the city of ana s ( ossetti et al. 2005
.A.A. Soares n blished data). At the s rface the
area containin the aleomor holo ies em hasized
here contains ate Pleistocene de osits that interce t
older Pleistocene strata of the Içá Formation (Fig.
3A). In addition Proterozoic crystalline roc s
bo nd these de osits to the so th and so theast.
Simpli ed geological map of the study area and its surroundings, with the Aripuanã-Marmelos and Jiparaná areas
indicated by rectangles (dashed line I-II indicates the position of a topographic pro le derived from DEM-SRTM shown in ).
DEM-SRTM topographic pro le (see location in ) ill stratin the
er and lower terrains in the Ari an - armelos area.
y sometic ma of the st dy area and its s rro ndin s. (Blac oly ons st dy areas).
he data sed in this research consist of freely
accessed remote sensin
rod cts incl din
andsat 5ima es (access on www.d i.in e.
br )
-S
data (access on ft ://e0sr 01 .
ecs.nasa. ov/srtm/) o tical ima es derived from
eolo ic and eomor holo ic
oo le arth
data available in the literat re and modern
draina e networ (scale 1:100 000) available in
shape le format from the Ministério do Meio
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
Ambiente (htt ://ma as.mma. ov.br/ma as/a lic/
cartoamazonia/). andsat 5ima es from
the year 2000 were selected based on low clo dcover and their corres ondence with the time
when the SRTM ight took place. These images
were re istered rocessed for (red) ( reen) B
(bl e) band com osition and inte rated with the
draina e networ . Several band com ositions were
erformed with the 5( ) ( ) and 3(B) rovidin
the best view of the feat res characterized herein.
he
-S
data derive from the ori inal
90-m resol tion (3 arc seconds) C-Band synthetic
a ert re radar data ac ired by the National
Aerona tics and S ace Administration (NASA)
National Ima ery and a in A ency (NI A)
( erman S ace A ency) and ASI (Italian
S ace A ency) aboard the s aceshi
ndeavo r
in February 2000. The data, downloaded from the
site htt ://edc. s s. ov/srtm/data/obtainin data.
html are n ro ected with eo ra hic coordinates
as reference nits and
S8 as the reference
elli soid and dat m. levation is e ressed in
meters. Ori inal
-S
resents data fail re
s ch as ne ative elevation val es es ecially in
areas of la es and rivers. his was corrected sin
the o o ra hy tool in the N I software for
re lacin bad val es. he
-S
data were
rocessed sin c stomized shadin schemes and
alettes (cf. ossetti and aleriano 2007 antelli
et al. 2009 aya awa et al. 2010) sin the lobal
a er software. his roced re was artic larly
sef l for hi hli htin the mor holo ical feat res
of interest for this research accordin to on-screen
observations. he mor holo y was also revealed
by ro hness from the
which hel ed
hi hli ht different roc s and de osits. he S
topographic pro les were useful in detecting
relief con guration and the main features and
forms. Inte ration of these data with available
eolo ical and eomor holo ical data hel ed
characterize and analyze the aleomor holo ies
of the st dy area.
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
he analysis of mor hostr ct ral lineaments
was based on eolo ical ma s rovided by the
Brazilian Instit te of eo ra hy (IB ) with
vector ad stments based on the analysis of remote
sensin
rod cts. he beeter characterization of
mor hostr ct ral lineaments consisted of vis al
inter retation and man al vectorization based on
1:100 000 modern draina e networ . O tical ima es
improved the identi cation of morphostructural
lineaments. ectorization and dia rams of absol te
fre ency and len th fre ency were develo ed
in the SRING 4.3.3. software. The identi cation
of draina e anomalies was based on vis al
inter retation of remote sensin data inte rated
with the modern draina e networ as s ested in
the literat re (e. . oward 1967 Sch mm et al.
2000). oo le arth ima es were sed to analyze
the feat res of interest in more detail.
The study area occurs in two terrains (Fig. 3A-C).
The rst is an area to the southeast with altitudes
between 100 and 150 m. Precambrian to Cretaceo s
roc s dominate in this area with aternary de osits
occ rrin only alon river valleys. he second area
to the northwest dis lays altit des ran in from 60
to 100 m and contains only
aternary de osits.
he contact between these terrains is shar and
consists of several straight segments which de ne
main N -trendin mor hostr ct ral lineaments.
Paleodraina e mor holo ies are recorded by
n mero s narrow b t elon ated belts that ran e
from strai ht to hi hly sin o s similarly to the
morphology of many modern uvial channels
(Fig. 4A-F). The paleomorphologies are either
contin o s or discontin o s the latter consistin
of sets of se ments rom tly reconstr cted as
aleochannel fra ments. In o tical ima es these
landforms are only detected where hi hli hted by
ioneer ve etation and/or bare soil in shar contact
with adjacent areas of dense forest (Fig. 4A-C).
In addition SPO ima es revealed that arts of
A
A
NA
the paleochannels are covered by sand dunes (Fig.
3 - ). Interestin ly tree s ecies from forested areas
ad acent to the belts are rad ally advancin toward
the paleochannel areas (Fig. 4F). In contrast to
IA
NA ICS IN A A ONIA
o tical ima es
-S
rovided a m ch more
com lete view of the st died aleomor holo ies
artic larly those hidden nder the dense rainforest
(Fig. 5A-B).
Characteristics of the aleochannels in the st dy area.
SPO ima e ( oo le arth ) ill stratin the shar contact
between ioneer formations over aleochannel areas and ombro hylo s forest in their s rro ndin s (inside bo es identify and .
SPO ima es ( oo le arth ) with details of the aleochannels shown in .
eneral view
and details
of a aleochannel covered by sand d nes (li ht tones) in shar contact with ombro hylo s forest (dar tones). Note in and
that the aleochannels are artly covered by forest (li ht tones in to
aleochannel with ioneer formations dar tones in
to
ombro hylo s forest). (See location of and in Fig. 3).
he aleomor holo ies in the st dy area can
be described as two aleochannel sets one located
between the Ari an and armelos ivers and the
other located in the lowest reaches of the i aran
River near its con uence with the Madeira River
(Fig. 3A). Paleochannels in the Aripuanã-Marmelos
inter uve are the largest ones and consist of an
intricated draina e networ that s reads o t over
an area
to 30 000 m2 (Figs. 6, 7A-C). These
aleomor holo ies occ r in both the hi hest
and the lowest terrains altho h they are more
wides read in the latter. he to o ra hy in the
lowest terrain enerally varies sli htly between 80
and 60 m northeastward (Fig. 3B). The dimension
of individ al aleochannels varies with len ths
to 250 m and widths
to 3.5 m. he lar est
paleochannels occur in the center of this area (Figs.
6 7A). hey form se ments that either interce t
laterally ad acent aleochannels or are arran ed as
interconnectin branches. here are downstream
conver ences to the northwest north and northeast
and aleochannel s er osition is common. A
stri in characteristic in the central art of the
st dy area is an assembla e of northwestward to
northeastward trendin dendritic aleodraina e
com osed of lar e (i.e. avera in 2.5 m in width)
aleochannels covered by ioneer ve etation.
hese aleochannels abr tly ta er downstream
as they conver e into sin le and hi hly sin o s
aleochannels that are in contin ity with active
channels (Fig. 7B). It is interesting that these
chan es occ r ri ht at the bo ndary between the
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
. OSS
I
iews of aleochannels com arin andsat ima es
with the
-S
. Paleochannels
covered by ioneer formations (arrows) are seen on both rod cts while aleochannels covered by dense
ombro hylo s forest are barely visible in the andsat ima e b t can easily be traced in the
-S
rod ct
(dashed line in ). (See location in Fig. 3).
revio sly described hi hest and lowest terrains.
Also remar able is that the channels have
orthogonal in ections at this boundary, and deviate
to the ri ht to follow the strai ht N -trendin
lineaments between the two to o ra hic terrains
(Fig. 7B). Another important morphological
observation is that the main aleochannels in
this area are hysically connected to the modern
An Acad Bras Cienc (2015) 87 (1)
Aripuanã River at several locations (Figs. 7A and C).
he connection of the main aleochannel in the
central art of this area occ rs where the Ari an
River develops an anomalously wide loop (Fig. 6).
he i aran
iver aleomor holo ies are
less e tensive than the ones in the Ari an armelos area encom assin less than 8 500 m2
(Fig. 8A-C). However, similarly to that area, most
A
A
NA
IA
7
NA ICS IN A A ONIA
Paleomor ho ies and the distrib tion of the hi hest and lowest terrain in
the Aripuanã-Marmelos inter uve. Note the sharp contact between the higher and
lower terrain (black arrows), de ned by straight NE-SW trending morphostructural
lineaments (dashed lines). Observe also the termination of several dentritic
northwestward owing paleochannels at this boundary and the many locations
where a aleochannel oins with the Ari an
iver (white arrows). (circle
anomalo s meander of the Ari an iver).
of the i aran
aleochannels are concentrated
in the lower terrain (Fig. 8D). Transverse DEMSRTM topographic pro les generally do not reveal
any signi cant altitudinal gradients, although an
overall northeastward to o ra hic variation from
90 to 100 m occ rs near the adeira iver. he
contact between the to o ra hically lower and
hi her terrains in the i aran area is also shar
being de ned by major straight and orthogonal,
NW-SE to NE-SW trending lineaments (Fig. 8A).
An Acad Bras Cienc (2015) 87 (1)
8
ICSON . A A A A and I C
. OSS
I
7
-S
ill stratin details of aleochannels in the central art of Ari an armelos area.
eneral view of intricate aleochannels (dotted lines) s er osed on
one another. Observe the aleochannels that terminate (arrows) at the bo ndary between the
hi her and the lower terrain. (bl e lines main modern channels inside rectan le locates B
circle a main aleochannel that oins an anomalo s meander of Ari an iver ).
etail
of A ill stratin three of the aleochannels that end at the bo ndary between the hi her and
lower terrains. Note that a modern northwestward owing channel associated with one of these
paleochannels locally in ects to the northeast and then back to the northwest, con guring
ortho onal an les (circle).
etail of the aleochannel that are interce ted by the Ari an
River where it con gures an anomalous meander in the southern part of this area. (See location
of and in Fig. 6).
An Acad Bras Cienc (2015) 87 (1)
A
A
NA
IA
NA ICS IN A A ONIA
8 Characterization of aleochannels in the i aran area.
-S
data with eneral view of
paleochannels (dashed red lines) on both sides of Jiparaná River (inside boxes locate gures
and most of
white lines I-II and III-IV locate topographic pro les shown in contin o s red lines strai ht mor hostr ct ral
lineaments located at the bo ndary between the hi hest and the lowest terrain).
-S
data with a closeof aleochannels (arrows) shown in the northwest art of .
ine drawin of the aleochannel networ .
Topographic pro les derived from DEM-SRTM (see location in .
-S
data with a detail of
ill stratin the interce tion of an almost N-S trendin aleochannel by a N -S
aleochannel where the
modern i aran iver is entrenched (yellow dashed lines
aleochannels) (circle interce tion oint dashed
yellow lines
aleochannels).
-S
data with a detail of A ill stratin the location where the co rse of
Jiparaná River (1) changes drastically from northeast to southwest, con guring a tight meander likely due to river
capture. Note a paleovalley (2) that indicates the previous course of this river, today occupied by a northeast owing
trib tary of the oosevelt iver (3).
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
owever aleochannels are less ab ndant than
in the Ari an - armelos area bein re resented
mainly by belts with len ths and widths
to 100
m and 3.6 m res ectively. hese feat res are
sli htly sin o s mostly contin o s and re resented
e cl sively by sin le belts arran ed in a radial attern
(Fig. 8A-C). Similar to many of the Aripuanãarmelos
aleochannels the mor holo ical
relationshi s of the i aran aleochannels attest
that they are s er osed on one another which
res lts in a misleadin im ression of branchin
channels.
stream all aleochannels conver e
into an area where the i aran
iver dis lays
anomalous meanders (Fig. 8E). It is noteworthy
that some of the aleochannels are s er osed
by the modern i aran iver which in the st dy
area is mostly strai ht to sli htly sin o s. All
aleochannels in the i aran area occ r northwest
of the oint where this river e eriences an
orthogonal in ection from northeast to northwest,
which result in a wide and closed meander (Fig.
8F). At this location, a tributary of another river,
the oosevelt iver is entrenched within a N -S
aleovalley connected to the i aran iver.
or hostr ct ral lineaments are similar
thro ho t the st dy area inde endently of the
eolo ical s bstrate as shown by the len th and
frequency diagrams presented in Fig. 9. The
orientation was the most common mode
followed by N -S
and N -S orientations.
N-S orientation was e ressive in the area corresondin to Precambrian basement roc s.
C
ANN
NA ICS O
I
he observation of aleochannels in the Ari an armelos and i aran areas is not a novelty. wo
revio s
blications (i.e.
a ro et al. 1978
atr besse 2002) rovided eneral descri tions of
these landforms. Additionally other aleochannels
were doc mented alon the adeira iver stream
from the study area (Souza Filho et al. 1999).
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
owever o r a roach based on
-S
data
allowed these aleochannels to be characterized
in more detail. his is artic larly tr e for aleochannels hidden nder dense forest which were not
detected by any other remote sensin rod cts. he
DEM-SRTM technology signi cantly enhanced
the otential for aleochannel scr tiny enablin a
better nderstandin of their tem oral relationshi s.
An observation of remar able interest rovided
by the e ce tional view of aleomor holo ies
revealed by
-S
was that most of the
main aleochannels in both areas were not coeval
in time. his is indicated by the intricate networ
of aleochannels that fre ently s er ose one
another rather than re resentin laterally coe istin
draina e systems. ost li ely these feat res record
sin le channels that occ ied different locations over
time. he reconstr ction of the Ari an - armelos
aleodraina e s ests the e istence of two main
north/northwest-trendin trib tary systems related to
ancient co rses of the Ari an and oosevelt rivers
(Fig. 10A). The convergence of these paleochannels in
the central art of this st dy area res lted in them bein
inter reted as trib taries connected to a sin le tr n
river that owed into the Madeira River. Following
a slight northwestward (Fig. 10B) migration, the
Ari an
aleoriver drastically chan ed into its
modern northeast-trendin co rse. As this rocess
occ rred the oosevelt iver was ca t red by a north/
northeastward owing river segment, which made
the connection between this river and the Ari an
River (Fig. 10C). Consequently, two long channel
se ments became abandoned to the west of the
Aripuanã River (Fig. 10C). In addition, the central
art of the st dy area became the headwater for
many northwestward small draining basins (Fig.
10 ) that were abandoned or are still in the
rocess of abandonment. he n mero s dendritic
northeastward trendin
aleodraina e systems
that occ r between the lowest and hi hest terrains
erha s were ossibly also abandoned d rin
this eriod.
A
A
NA
IA
NA ICS IN A A ONIA
or hostr ct ral lineaments from the st dy areas (indicated by the oly ons) and its s rro ndin s. Incl ded
rose dia rams shows lineament fre ency and len th from areas of Precambrian basement roc s and sedimentary de osits
corres ondin to the entire re ion.
es ite the less intricate networ the aleochannel dynamics in the i aran area is not as well
nderstood as those from the Ari an - armelos
area. All the i aran aleochannels have a common
root with the downstream se ment of the modern
i aran iver. hey s read o t northwestward from
this river following a radial pattern. For this reason,
a reliminary im ression is that these aleochannels
record several distrib taries. owever the
S
data did not rovide any evidence to
s ort a myriad of laterally coe istin channels
ty ical of distrib tary systems. Instead these
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
. OSS
I
Pro osed draina e evol tion in the Ari an - armelos area based on inter retation of aleochannel
relationshi s derived from the
-S
. A set of av lsion e isodes c lminated with the dislocation of Ari an iver
from northwest to northeast. ( ime increases from to
dashed lines
aleochannels strai ht lines in the center of the
strai ht mor hostr ct ral lineaments between the hi her and lower terrains). (See te t for f rther e lanation).
An Acad Bras Cienc (2015) 87 (1)
A
A
NA
aleochannels more li ely record different ositions
occ ied by a sin le channel in this instance the
lower Jiparaná River (Fig. 8C). Hence, the most
robable hy othesis is that this river was located
nearly 60 m eastward of its modern osition
(measured at the con uence with the Madeira
iver) when it drained northward. his river was
then dislocated bac and forth several times ntil it
ended in its resent northwest osition. As mi ration
too
lace revio sly abandoned co rses were
ro ressively s er osed by active channels. his
dynamic evol tion wo ld have rod ced the radial
aleodraina e networ and the associated trian larsha ed sedimentary s ccession.
A
ISI
O
EGAFAN
O
Considerin the recedin disc ssion of channel
dynamics over time the new data resented here
can be sed to review their revio s attrib tion to
me afan systems (cf. atr besse 2002
il inson
et al. 2010). Megafans are generally de ned as
de ositional systems of reat dimensions i.e. 103-105
m2 ( eCelles and Cavazza 1999) develo ed in areas
of very low to o ra hy i.e. 0.1 to 0.01 ( ohain
and Parkash 1990, Sinha and Friend 1994, Leier et al.
2005) mostly nder arid to semiarid climate ( iblin
2006). his ty e of de ositional system rod ces lar e
scale sediment de osition mainly by the develo ment
of multiple distributary channels (Friend 1978, Kelly
and Olsen 1993, Nichols and Fisher 2007, Hartley
et al. 2010 eissmann et al. 2010). Accordin to
these a thors channels associated with me afans are
either meanderin or braided and they may rod ce
large amounts of uncon ned fan-shaped deposits.
his characteristic im oses an overall trian lar
mor holo y to the entire system.
rian lar or fan-sha ed de osits and distrib tary
channel patterns have generally been used to de ne
me afans (e. .
mbricht et al. 2001 Stanistreet
and cCarthy 1993 Sinha et al. 2005 Nichols and
Fisher 2007, Chakraborty et al. 2010). Fan-shaped
de osits and ne ivocal feat res s ortin
IA
NA ICS IN A A ONIA
multiple distributary networks were not identi ed in
the st dy areas. As demonstrated above the st died
landforms are more consistent with a few channels
that chan ed their co rse over time rather than
laterally coe istin interconnectin distrib tary
channels. In fact many aleochannels s
osedly
related to distrib tary aleochannel networ s
act ally res lt from s ccessive av lsions of a sin le
channel over time. he channel bif rcations of the
Aripuanã-Marmelos area suggest downstream ow
conver ence rather than a diver ence as wo ld be
e ected from distrib tary channels.
The conceptual model of uvial distributaries
has been sed to characterize me afan systems since
its introduction by Friend (1978). Such a model
cannot be a lied to s ort a me afan hy othesis
for the st dy areas. Instead the st died aleodraina e
systems a ear to corres ond to a small n mber of
trib taries that nderwent av lsions and ca t res
over time. O r inter retation is that this radial
paleodrainage arrangement re ects dislocation of a
few main trib taries of the adeira iver.
O r st dy of the adeira aleomor holo ies
led to a re-eval ation of the se of the term me afan to
refer to de ositional systems. his term corres onds
to an assembla e of enetically related lithofacies
within a artic lar de ositional environment which
is de ned, in turn, as a geomorphic unit formed by
laterally coe istin s b-environments. he st dy of
de ositional environments in the ancient record is
therefore essentially the st dy of eomor holo y
i.e. the reco nition of eomor hic nits where
sediment de osition ta es lace ( einec and
Sin h 1986). In the artic lar case of o r st dy
area there is no evidence to s ort neither clearlyde ned cone-morphologies with correspondence to
eomor hic nits nor hysical rocesses distinct
from those related to uvial systems. In addition to
the absence of distrib tary channel networ s there
is no indication of a conve - fan mor holo y
that may have ind ced channel shiftin from one
osition to another.
hile aleochannels may
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
be radially distrib ted (at least in the case of the
i aran area) they do not seem to be associated
with fan-sha ed de osits. On the contrary the
most likely interpretation is that the channel ows
were never distrib ted as a conse ence of a fan
mor holo y. ence what most li ely occ rred
was that as trib tary channels shifted osition
along a at-lying area, temporally distinctive
uvial sedimentary successions built up laterally or
s er osed on one another in order to establish a
sedimentary record (not a eomor hic nit ) with a
trian lar mor holo y in lan view.
he fore oin inter retation of the adeira
aleodraina e com le es is in a reement with observations from several other megafan analogs. For
instance the osi iver fan one of the most wellst died me afan worldwide was b ilt by n mero s
av lsions ( oo er ea 1961 ohain and Pra ash
1990 Brid e 2003) with several shifts over time
(Sinha 2009 Cha raborty et al. 2010). he modern
channel of this river in the fan area dis lays an
anastomosin attern and this occ rs where av lsion
channels re oin the main stream (Slin erland and
Smith 200 ). Ass min this as a modern analo for
the aleochannels recorded in that area the fan as a
whole may have been b ilt thro h artial av lsions
instead of f lly distrib tary channels radiatin
from a trunk river. Other distributary uvial fans
have been re-inter reted as de ositional settin s
characterized by m lti le av lsions of trib tary
channels and not by downstream bif rcation of
tem orally coe istin channels (e. . North and
arwic 2007 Bernal et al. 2011).
ore than a sim le matter of semantics this iss e
is of reat relevance when analyzin me afans and
attem tin to reconstr ct their sedimentary record.
Sedimentary lithofacies rod ced in me afans
lacking true evidence of both distributary ows and
associated uncon ned fan deposits are compared to
those lithofacies produced in uvial environments
with fre ent av lsions b t not necessarily
associated with lan view fan mor holo ies. he
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
-S
to o ra hic radient s ests a
northeastward-di in terrain in the Ari an area
and a nearly horizontal terrain over most of the
i aran area. In addition to the lac of evidence
for distributary ows, the Jiparaná area does not
show sedimentary s ccessions with conve - fan
mor holo ies as doc mented in ty ical me afans
s ch as the O avan o ( mbricht et al. 2001) the
a ari (Assine 2005) the osi (Cha raborty et al.
2010) and the Pastaza (Bernal et al. 2011). In art
this co ld mean that the fan mor holo y was cleared
from the landsca e after fan abandonment. owever
the hy othesis that a conve - fan mor holo y was
never established in the st dy areas sho ld not be
r led o t. he referred inter retation is that the
radial aleodraina e mor holo y observed in remote
sensin rod cts in this instance is d e to trib tary
channels that e erienced av lsions over time.
A
SION
I
C ANIS
Av lsion is most often ca sed by ra id all viation
d e to hi h sediment load trans orted into the
main channel, when
oodplain aggradation
increases (Slin erland and Smith 200 ). owever
other causes may also exist, such as changes in ow
dischar e to o ra hy s bsidence rate draina e
catchment size and channel radient. A radation
may be tri ered by mechanisms intrinsic to the
depositional environment, such as high oods, but
fre ent av lsions are more common in tectonicallyin uenced geological settings (e.g., Schumm et al.
1996 ones and Sch mm 1999
mbricht et al.
2001 Assine 2005) and are artic larly recorded
in foreland basins ( orton and eCelles 2001
Leier et al. 2005, Nichols and Fisher 2007).
ifferent ro ies have been resented in
s ort of dry climatic e isodes d rin the ate
Pleistocene in Amazonia (Absy et al. 1991 ebb
and ancy 1996 Behlin et al. 1999 Pessenda et
al. 2001 Sifeddine et al. 2001). he revio sly
ro osed me afans in the adeira area were lin ed
to dry climatic hases d rin the ast lacial
A
A
NA
a im m with s bse ent channel abandonment
followin sta es of climate amelioration ( atr besse
2002). his inter retation is valid only nder two
ass m tions: (i) the aleodraina e networ s are
related to me afan mor holo ies and (ii) me afans
are indeed restricted to arid and semi-arid areas. In
addition to data from modern h mid to s bh mid
me afans (for instance the a ari me afan
described by Assine 2005) the disc ssion resented
herein leads s to ar e that climate mi ht have not
been the main tri er of trib tary channel av lsions
recorded in the adeira area.
Although a de nitive interpretation will require
f rther eolo ical validation a line of mor holo ical
evidence s orts tectonics as the most la sible
ca se of channel av lsion in the Ari an - armelos
and i aran areas. vidence that the
aternary
de osits in these areas were formed in a low-lyin
terrain d e to fa lt s bsidence incl des: (i) its shar
contact with Precambrian to Cretaceous rocks de ned
by several N -trendin strai ht mor hostr ct ral
lineaments (ii) the matchin of these lineaments
with the abr t narrowin of several lar e N - to
N -trendin aleochannels which s ests chan es
in river co rses d e to terrain dis lacement and
(iii) the many draina e anomalies consistin of N trending orthogonal river in ections at the boundary
between the lower and hi her terrains. Additionally
tectonic tiltin is indicated by the overall N di in
-S
to o ra hic radient of these
terrains. his inter retation is consistent with both
the dislocation of the Ari an iver from a N/N trend to its modern northeast position (Fig. 8A-D) and
the overall ro ressive northeastward develo ment
of av lsion channels. he wide loo coincident with
the av lsion a is of the Ari an iver constit tes
a ma or draina e anomaly f rther s ortin
tectonically-controlled river shifts. Furthermore,
the abrupt orthogonal in ection of the modern
lower co rse of the i aran iver from northeast to
northwest (Figs. 1A, 3A), added to its association to
a wide and ti ht meander constit tes an im ortant
IA
NA ICS IN A A ONIA
draina e anomaly f rther s estive of tectonic
in uence. In this location, the entrenchment of the
oosevelt iver s trib tary within a aleovalley
connected to the i aran
iver indicates that the
latter river ran northeastward before deviation to
its modern northwest osition. A revio s re ional
investi ation s ested that this river ca t re was
d e to tectonics (i.e. a ro et al. 1978). Alto ether
s ch mor holo ical characteristics lead s to ro ose
tectonics as the ca se of s ccessive shifts of the
lower co rse of the i aran iver from northeast
to northwest.
he mor holo ical characteristics of the st dy
areas do not constit te isolated feat res in s ort
of a tectonic in uence on the Amazonian lowlands
d rin the late aternary. any earlier blications
have emphasized this issue. For instance, an early
st dy reco nized that the middle Amazon iver
is controlled by N -S
and N -S trendin
fa lts (Sternber 1950). he lower Ne ro iver is
li ely a half- raben related to de tral - stri e
slip faults (Franzinelli and Igreja 1990), as well as
nearly E-W and N-S trending structures (Franzinelli
and atr besse 1993). ore recently it has been
ro osed that the c rrent lower co rse of this river
is driven by dis lacement alon re-e istin N -S
tectonic faults (Almeida Filho and Miranda 2007).
A combination of N -S N -S and - trendin
faults in the late Holocene in uenced channel
dynamics in the middle Amazon iver ( atr besse
and Franzinelli 2002). Closer to the study areas,
ma or river rearran ements in the P r s basin were
related to tectonic s bsidence (Pimienta 1958 Saadi
1993). Additionally the activity of re-e istin
fa lts wo ld have romoted the so theastward
dislocation of a nearly 200 m lon se ment of the
adeira iver as well as many associated draina e
anomalies immediately northwestward of the st dy
area ( aya awa et al. 2010). Channel abandonment
re orted in the
er adeira iver was related to
tiltin ca sed by tectonic reactivation of N -S
and NE-SW transform faults (Souza Filho et al.
An Acad Bras Cienc (2015) 87 (1)
ICSON . A A A A and I C
1999). N mero s other st dies have also s ested
tectonics as the most signi cant control of ancient
and modern river develo ment in Amazonian areas
(e. . a ro et al. 1978 Bemer y and Costa 1991
atr besse and ancy 2000 Costa et al. 1995 2001
Fernandes Filho et al. 1997, Nogueira and Sarges
2001, Franzinelli and Igreja 2002, E.A.A. Soares,
n blished data ossetti et al. 2007 2012a b see
also several references in ertes and nne 2007).
A recent
blication has demonstrated that the
development of uvial terraces along the Madeira
River occurred under the in uence of tectonics
( ossetti et al. 2013). he e tensive doc mentation
of tectonic in uences on Amazonian rivers is also
consistent with modern seismo enic data from this
re ion where earth a es of hi h ma nit des (
to 8) have been recorded (Ass m o and S rez
1988, França 2006).
he redominant orientation of the mor hostructural lineaments in the study area (see Fig. 9) is
in agreement with Precambrian shear zones de ned
re ionally in the Amazon Craton (Costa et al. 1996).
hese shear zones were reactivated d rin the
Neo ene- aternary and also affected sedimentation
in the Holocene (F.H.R. Bezerra, unpublished data).
hese to ether with the data resented herein
s ort a tectonically nstable Amazonian lowland
d rin the aternary with a direct conse ence on
the evol tion of its river systems.
he
-S
constit tes an im ortant tool
to im rove the characterization of aleodraina e
networ s in forested areas of Amazonia. his
ty e of data was f ndamental to analyze the
adeira aleodraina e networ s allowin s to
ro ose a com rehensive model that can e lain
channel dynamics d rin the late
aternary.
he com le sets of aleochannels resent in this
area were attrib ted to s ccessive av lsions of a
small n mber of channels over time. he radial
distrib tion of the st died aleochannel systems in
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
lan-view resembles distrib tary networ s related
to me afans. owever the st died de osits do
not contain evidence of distrib tary channels or
of their association with conve - de ositional
environments as ty ical of me afans.
he
present study reveals that large tributary uvial
systems s b ected to av lsions can be e ivocally
inter reted as distrib tary me afans. In both cases
the res ltin de osits dis lay fan sha es associated
with radial aleodraina e networ s. Considerin a
me afan model for the st dy areas this wo ld be
characterized by m lti le av lsions of trib tary
channels within a iven time scale rather
than by downstream bif rcation of tem orally
coe istin channels. S ch characteristic does not
conform to me afan models. he mor holo ical
characteristics of the st dy area indicate to tectonics
as an im ortant mechanism leadin to channel
shifting. Therefore, rather than climate uctuations
associated with lacial/inter lacial e isodes we
ro ose that channel shiftin over time and the
res ltin com le networ s of radially distrib ted
aleochannels were romoted by fa lt reactivation.
€
•
he a thors ac nowled e the Conselho Nacional
de Desenvolvimento Cientí co e Tecnológico
(CNP ) for a doctoral scholarshi and a research
fellowshi ( ro ect
71 83/06-0). he Instit to
Nacional de Pes isas s aciais (INP ) rovided
the com tational reso rces needed for rocessin
remote sensin data. e also wish to than the
Brazilian eolo ical S rvey-CP
and the 5 th
n le Infantry Battalion of the Brazilian Army for
logistical support during eldwork.
‚
€
Sistemas de drena em anti os têm sido doc mentados
na bacia do Amazonas e s a caracteriza o
para a reconstrução da evolução
cr cial
uvial nessa área.
Morfologias uviais, incluindo cinturões alongados, são
bem reservadas ao lon o do rio
adeira. O modelo
A
di ital de eleva o do
(S
A
e adar
NA
ra
IA
issi n
) favorece a detec o dessas fei es at mesmo
em áreas cobertas por vegetação orestal densa. Essas
aleomorfolo ias s o atrib das a m dan as de osi o de
anti os trib t rios do rio
ssas redes de
adeira or meio de av ls es.
aleodrena ens radiais
morfolo ias em le e
rod ziram
e lembram me ale es
distrib t rios. A distin o entre sistemas trib t rios
av lsivos e me ale es distrib t rios no re istro
sedimentar é um desa o. A paleodrenagem do Madeira
revela a s er osi o de canais trib t rios formados or
av ls es m lti las dentro de m dado er odo de tem o
mais do
e a bif rca o a sante de canais coe istentes.
A av ls o de canal nessa rea Amaz nica d rante o
atern rio tardio
relacionada
tect nica devido a
fei es como: (i) lineamentos retil neos coincidentes
com dire es de falhas (ii) mer lho
dos terreno com estratos
ara nordeste
atern rios e (iii) v rias
anomalias de drenagem, incluindo in exões ortogonais
de drena em. ssas caracter sticas em con nto levam a
ro or
e a aleodrena em radial resente nas mar ens
do rio
adeira res lta de av ls es s cessivas de canais
trib t rios ao lon o do tem o devido tect nica.
ƒ„…„† „‡ ˆ‰„† :
aleocanais Bacia Amaz nica rio
adeira sensoriamento remoto clima tect nica.
‚
‚
CLEEF A FO NI
A IN
S AN
SIFFEDINE A SI A MFF SO BI S F S
I
C
B AN
AN
A
N . 1991.
ise en vidence de
atre hases d o vert re de la forêt dense dans le s dest de l Amazonie a co rs des 60000 derni€re ann es.
Premi€re com arison avec d a tres r ions tro icales.
Com te end s l Acad Sci 312: 673-678.
I A FI O
AN
I AN A FP. 2007.
e a ca t re
A
of the io Ne ro and formation of the Anavilhanas
Archi ela o Central Amaz nia Brazil: evidences in na
S
di ital elevation model. em Sens nv 10: 387-392.
APO C NO N O AF AN S BON . 1988. A descoberta de
etr•leo do io r c Bacia do Solim es. In: Con r Bras
eol 2 1988. Bel m Brasil. Proceedin s...Bel m: Soc
Bras eol 6: 2‚16-2‚27.
. 2005. iver av lsions on the a ari me afan
ASSIN
Pantanal wetland Brazil. eomor holo y 70: 357-371.
ASS Pƒ„O AN S … † . 1988. So rce mechanisms of
moderate-size earth a‡es and stress orientation in midlate So th America. eo hys ˆ 92: 253-267.
ABS
NA ICS IN A A ONIA
7
IO ˆC AN
OO I S A . 1999. ate
B
aternary ollen records from the middle Ca et
river basin in central Colombian Amazon. Palaeo eo r
Palaeoclimatol Palaeoecol 1‚5: 193-213.
B
AN COS A ˆBS. 1991. Considera es sobre
a evol o do sistema de drena em da Amaz nia e s a
rela o com o arcabo o tect nico-estr t ral. Bol
s
Paraense m lio oeldi 3: 77-98.
B NA C C IS OP O F A O† S ˆ SO A ˆ-C AN
B
OS PB. 2011. ate lacial and olocene av lsions
of the io Pastaza e afan ( c ador-Per ): fre ency
and controllin factors. Int ˆ arth Sci 100: 1759-1782.
B ANI C OSS I DF AN A B
PC . 2013.
Object-based classi cation of vegetation and terrain
to o ra hy in so thwestern Amazonia (Brazil) as a tool
for detecting ancient uvial geomorphic features. Comp
eosci 60: ‚1-50.
B I
ˆS. 2003. Rivers and oodplains: forms, processes and
sedimentary record. Blac‡well Science td O ford 20‚ .
CAP O
AN SI A OB. 1990. Sedimenta o e tect nica
da Bacia do Solim es. In: AˆA ABA IA P
and I ANI ˆ ( ds) Ori em e evol o de bacias
sedimentares. Petrobras io de ˆaneiro . 169-191.
C A ABO
A
OS P AN BAS S. 2010. osi
me afan: historical record eomor holo y and the recent
av lsion of the osi iver. at Int 227: 1‚3-160.
COS A ˆBS B
AS I AN BO
S S. 2001.
ectonics and aleo eo ra hy alon the Amazon iver.
So th Am arth Sci 1‚: 335-3‚7.
COS A ˆBS AS I BO
S S AN B
. 1995.
Arcabo o tect nico esoz•ico-Cenoz•ico da re i o da
calha do rio Amazonas. eociências 1‚: 77-103.
C N A P C ON†A A FG CO IN O LFC AN F Iˆ‰ FJ.
199‚. Bacia do Amazonas. Bol eocienc Petrobras 8: ‚7-55.
A ON RF. 1975. Contribuição para a datação da Formação
Alter do Ch o Bacia do Amazonas. ev Bras eocienc
5: 78-8‚.
C
S P AN CA A††A Š. 1999. A comparison of uvial
me afans in the Cordilleran (
er Cretaceo s) and
modern imalayan foreland basin systems. eol Soc Am
B ll 111: 1315-133‚.
F NAN S FI O A COS A
AN COS A ˆBS. 1997.
e istros neotect nicos nos lateritos de
ana s Amazonas. eociências 16: 9-33.
F ANƒA S. 2006. Brazil seismicity. B ll Int Inst Seismol
arth a‡e n ‚0: 23-36.
F AN†IN I AN I
ˆA
S. 1990. tiliza o de sensoriamento remoto na investi a o na rea do Bai o rio Ne ro
e rande ana s. In: Sim Bras Sens em 6 1990.
ana s Brazil. Proceedin s... ana s: Soc Bras eol
3: 6‚1-6‚8.
F AN†IN I AN I
ˆA . 2002.
odern sedimentation
in the ower Ne ro iver Amazonas State Brazil.
eomor holo y ‚‚: 259-271.
F AN†IN I AN A
B SS
. 1993. he se of remote
sensin in a neotectonic st dy in the Amazon Basin.
B ll IN A 16: 10-13.
B
IN
An Acad Bras Cienc (2015) 87 (1)
8
F
ICSON . A A A A and I C
PF. 1978. istinctive feat res of some ancient river
systems. In: Miall AD (Ed), Fluvial Sedimentology. Can
Soc Petr eol emoir 5: 531-5‚1.
F I N PF. 1989. S ace and time analysis of river systems
ill strated by iocene systems of the northern bro Basin
in Ara on S ain. ev Soc eol s a a 2: 55-6 .
OO -S A
. 1972. Sedimentation of the
F I N PF AN
Wood Bay Formation (Devonian) of Spitsbergen: regional
analysis of a late or enic basin. Nors Polar Inst S rifter
157 Oslo 77 .
IB IN
. 2006. Width and thickness of uvial channel
bodies and valley lls in the geological record: a literature
compilation and classi cation. J Sed Res 76: 731-770.
IBBS
. 1967. he eochemistry of the Amazon
iver
system art. I. he factors that control the salinity and the
com osition and concentration of the s s ended solids.
eol Soc Am B ll 78: 1203-1232.
or holo y of the osi
O AIN
AN PA AS B. 1990.
me a an. In: AC OC I A and C
C
( ds)
Alluvial Fans, Wiley & Sons, London, p.151-178.
C. 2001. he
B IC
CCA
AN
o o ra hy of the O avan o elta Botswana and its
sedimentolo ical and tectonic im lications. So th Afric
eol 10 : 2 3-26 .
A
A
ISS ANN S NIC O S
AN
A
IC
. 2010. Large distributive uvial systems: characteristic
and controls on develo ment. Sed es 80: 167-183.
A A A A
OSS
I DF AN
A
IANO
. 2010.
A lyin
-S
for reconstr ctin a late aternary
aleodraina e in Amazonia. arth and Plan Sci ett
297: 262-270.
O ON B AN
C
S P . 2001.
odern and ancient
uvial megafans in the foreland basin system of the central
Andes so thern Bolivia: Im lications for draina e networ
evol tion in fold-thr st belts. Basin es 13: 3-61.
O A
A . 1967. raina e analysis in eolo ic inter retation:
A s mmation. Amer Assoc Petrol eol B ll 51: 22 6-2259.
I ION . 198 . Sedimentation and sediments of Amazonian
rivers and evol tion of the Amazonian landsca e since
Pliocene times. In: SIO I ( d) he Amazon limnolo y
and landsca e ecolo y of a mi hty tro ical river and its
basin. n P blishers ordbrecht . 201-21 .
IO . 1981. Neotectonics of the Amazon
I ION O AN S
lain. B ll IN A Neotect Commission : 72-78.
SA. 1999. Ca ses of av lsion: an
ON S S AN SC
overview. In: SMITH ND and ROGERS J (Eds), Fluvial
sedimentolo y. Blac well Science S ec P bl Int Assoc
Sed n. 28 O ford . 171-178.
SB AN O S N . 1993. erminal fans: a review with
reference to evonian e am les. Sed eol 85: 339-37 .
A
B SS
. 2002. vidence of
aternary alaeohydrolo ical chan es in middle Amaz nia: he Ari an Roosevelt and Jiparaná “fans”. Z Geomorph NF129: 61-72.
A
B SS
. 2008. Patterns of Anabranchin channels:
the ltimate end-member ad stments of me a-rivers.
eomor holo y 101: 130-1 5.
I N
An Acad Bras Cienc (2015) 87 (1)
. OSS
I
B SS
AN F AN IN
I . 2002. he
olocene
all vial lain of the middle Amazon iver Brazil.
eomor holo y : 2 1-257.
A
B SS
AN
A ON
C. 199 . A Climatic odel
for So thwestern Amazonia at ast lacial times.
at
Int 21: 163-169.
A
B SS
AN
ANC A. 2000. Neotectonic in uence
on tro ical rivers of so thwestern Amazon d rin the late
aternary: the oa an I i na river basins Brazil.
at Int 72: 67-72.
A
B SS
S A
C AN SIN A . 2005. ro ical
ivers. eomor holo y 70: 187-206.
I A
C
S P AN P
I
. 2005. o ntains
monsoons and me afans. eolo y 33: 289-292.
AN
I
OSS
I DF A B
P AN
A
IANO
. 2009. A lyin S
di ital elevation
model to nravel aternary draina e in forested areas in
northeastearn Amazonia. Com eosci 35: 2331-2337.
A O CA N N S B A AN
F ANCO
S . 1978.
Geomorfologia-Folha SB 20 Purus. RADAMBRASIL,
NP
io de aneiro.
S A AN
NN
. 2007. ffects of tectonism climate
chan e and sea level chan e on the form and behavio r of
the modern Amazon River and its oodplain. In: GUPTA
A ( d) ar e rivers: eomor holo y and mana ement.
Wiley & Sons, United Kingdon, p. 115-144.
ONSC
A. 1998. Miocene sh faunas from the northwestern
Amazonian basin (Colombia Per Brazil) with evidence of
marine inc rsions. Palaeo eo r Palaeoclimat Palaeoecol
1 3: 31-50.
OO
A . 1961. he osi-a challen e in river control.
o rnal of the Instit tion of n ineers (India) 2: 117-1 2.
I ION
O N AN
N
. 1995.
ydrolo ical chan es of the Amazon d rin the ast
lacial-Inter lacial Cycle in Central Amazonia (Brazil).
Nat rwissenschaften 82: 232-235.
AN FIS
A. 2007. Processes facies and
NIC O S
architecture of uvial distributary system deposits. Sed
eol 195: 75-90.
I A AC AN SA
S
. 2001. Characterization and
NO
genesis of waterfalls of the Presidente Figueiredo region,
northeast State of Amazonas Brazil. An Acad Bras Ciênc
73: 287-301.
CP AN
A
IC
. 2007. Fluvial fans: myths,
NO
misconce tions and the end of the terminal fan model.
Sed es 77: 693-701.
A A NA
OSO N
O
IA
P SS N A C BO
S
IB I O AS AN
A O
. 2001. Ori in and
dynamics of soil or anic matter and ve etation chan es
during the Holocene in a Forest-savanna transition zone,
Brazilian Amazon re ion. olocene 11: 250-25 .
PI I N A . 1958. Modi cations climatiques et subsidence
r cent affectant le lacis s d d Bassin de l€ Amazone.
C Acad Sci 2 6: 2268-2271.
IN C
AN SIN
IB. 1986. e ositional Sedimentary
nvironments 2nd ed. S rin er- erla Berlin 579 .
A
A
A
NA
I DF. 2010.
lti le remote sensin techni• es as
a tool for reconstr ctin late
aternary draina e in the
Amazon lowland. arth S rf Proc andf 35: 123 -1239.
OSS
I DF B
ANI
C ANI
C
ON
AN
A A A A
. 2012b.
ate
aternary sedimentary
dynamics in estern Amazonia: Im lications for the
ori in of o en ve etation/forest contrasts. eomor holo y
177: 7 -92.
OSS
I DF CO N C B
ANI C A A A A
PA
S CAS O DF AN F IA S . 2013. ate
aternary
uvial terrace evolution in the main southern Amazonian
trib tary. Catena 116: 19-37.
OSS
I DF AN N
O
. 2006. First Evidence of Marine
In uence in the Cretaceous of the Amazonas Basin,
Brazil. Cret es 27: 513-528.
OSS
I DF
O
O P
AN
‚ S A . 2005. New
eolo ical framewor for estern Amazonia (Brazil) and
im lications for bio eo ra hy and evol tion.
at es
63: 78-89.
OSS
I DF AN
A
IANO
. 2007. vol tion of the
lowest Amazon basin modeled from the inte ration of
eolo ical and S
to o ra hic data. Catena 70: 253-265.
OSS
I DF
A
IANO
AN
A
S
. 2007. An
abandoned est ary within ara Island: im lications for
ate aternary aleo eo ra hy of northern Brazil.
st
Coasts 30: 813-826.
OSS
I DF ANI
CO N C AN C
ON
. 2012a.
A ate Pleistocene- olocene wetland me afan in the
Brazilian Amazonia. Sedim eol 281: 50-68.
SAA I A. 1993. Neotect nica da Plataforma Brasileira: esbo o
e inter reta o reliminares. ev Bras eocienc 1: 1-15.
SC
SA
ON JF AN
O B OO
. 2000. Active
tectonics and all vial rivers. Cambrid e niv Press
elborne 276 .
SC
SA S IN
AN
I
A
. 1996. or holo y
hydrolo y and evol tion of the anastomosin Ovens and
in ivers A stralia. eol Soc Am B ll 108: 1212-122 .
SIFEDDINE A
A IN
C
B
O
- IB I O
C SO BI S F CO
I O
C AN S
IO
. 2001.
ariations of the Amazonian rainforest environment:
a sedimentolo ical record coverin 30 000 years.
Palaeo eo r Palaeoclimat Palaeoecol 168: 221-235.
SI A C
O A S N C S A AP COS A SS AN
A
.
2007. Analysis of tectonic-controlled uvial morphology
and sedimentary rocesses of the western Amazon basin:
an a roach sin satellite ima es and di ital elevation
model. An Acad Bras Cienc 79: 693-711.
SIN A . 2009. he reat av lsion of osi on 18 A
st 2008.
C rrent Science 97: 29- 33.
SIN A
AN F I N PF. 199 .
iver systems and their
sediment ux, Indo-Gangetic plains, Northern Bihar,
India. Sedimentolo y 1: 825-8 5.
OSS
IA
NA ICS IN A A ONIA
SIN
A
IB IN
AIN
AN
AN ON S . 2005.
Sedimentolo y and av lsion atterns of the anabranchin
Ba hmati iver in the imalayan foreland basin India.
S ec P b Int Assoc Sed 35: 181-196.
SIO I . 198 . The Amazon and its main a uentes:
ydro ra hy mor holo y of the ivers co rses and
river ty es. In: SIO I
( d) he Amazon: limnolo y
and landsca e ecolo y of a mi ht tro ical river and its
basin. n P blishers Netherlands . 127-166.
S IN
N . 200 . iver av lsions and
AN
AN S I
their de osits. Ann ev arth and Plan Sci 32: 257-285.
SO A FI O P
A OS
S SCAN O A A FI O
PS AN
IS
. 1999. Com artimenta o morfoestr t ral
e neotectônica do sistema uvial Guaporé-Mamoré-Alto
adeira ond nia Brasil. ev Bras eocienc 29: 69- 76.
S ANIS
CCA
I AN
S. 1993. he O avan o
Fan and the classi cation of subaerial fan systems. Sed
eol 8: 115-133.
S
O. 1950. ales tect nicos na lan€cie amaz nica•
NB
ev Bras eo : 511-531.
I‚ I A
ASSINA I CC CO ANI
AN
A AS I A
. 1989. A review of the eochronolo y of the Amazonianian
Craton: tectonic im lications. Precamb es 2: 213-27.
I A
AN S A
. 2000.
owermost Amazon
River: evidence of late Quaternary sea-level uctuations
in a com leƒ hydrodynamic system. at Int 72: 53-60.
BB S AN
ANC A. 1996. ate Cenozoic evol tion of
the Neotro ical mammal fa na. In: AC SON B
N and COA S A ( ds) vol tion and nvironments in
ro ical America. niversity of Chica o Press Chica o
. 335- 11.
ISS ANN S
A
A NIC O S
SC
I A
AN BAN A
. 2010. Fluvial form
O SON B
in modern continental sedimentary basins: istrib tive
uvial systems. Geology 38: 39-42.
SS IN
FP
„S„N N
I ION
ONHOF
B
AAN O P
N A
O
O-PI
AN
AN
IN AS
. 2001.
a e Pebas: a alaeoecolo ical
reconstr ction of a iocene lon -lived la e com leƒ in
western Amazonia. Cainoz es 1: 35-81.
I
INSON
I
A S A
N B
AN
e afan environments in northern
So th America and their im act on Amazon Neo ene
a… atic ecosystems. In: OO N C and
SS IN
FP (Eds), Amazonia: landscape and species evolution.
Blac well P blishin
alasia . 162-18 .
IA S A. 2000. Flexural cantilever models of extensional
s bsidence in the
nster Basin (S Ireland) and Old ed
Sandstone uvial dispersal systems. In: FRIEND PF and
I IA S P ( ds) New ers ectives on the Old ed
Sandstone. eol Soc ondon S ec P bl 180: 239-268.
S A S
. 2010.
An Acad Bras Cienc (2015) 87 (1)