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INSTITUTO DE QUIMICA
'- DOUTORADO EM GEOQUIMICA AMBIENTAL
SEDIMENTACAO EM ECOSSISTEMAS DE MANGUE:
ESTABILIDADE, APLlCAC;OES E ESTOCAGEM DE
CARBONO EM RELAC;Ao AO NIVEL DO MAR
'NITEROI
. 2009
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tJ~nVEPJSDADE FEDERAL FLUMlNENSE
INSTITUTO DE QUIMICA
DEPARTAMENTO GEOQillMICA
SEDIMENTA<;AO EM ECOSSISTEMAS DE MANGUE: ESTABILIDADE,
APLICACOES E ESTOCAGEM DE CARBONO EM RELA<;AO AO
NlVELDOMAR
NITEROI
2009
ads:
SEDlMENTA<;AO EM ECOSSISTEMAS DE MANGUE:
ESTABILIDADE, APLICA<;OES E ESTOCAGEM DE
CARBONO EM RELA<;AO AO NiVEL DO MAR
Tese apresentada ao Curso de P6s-Graduac;ao em
Geociencias da Universidade Federal Fluminense,
como requisito parcial para a ·obtenc;ao do Grau
de Doutor. Area de Concentrac;ao: Geoquimica
Ambiental.
ORlENTADOR: Prof. Dr. SAMBASIVA RAO PATCHINEELAM
CO-ORIENT ADOR: Prof. Dr. JOSEPH M. (DONNY) SMOAK
NITERor
2009
[
I
I
1
I
f ~_
S215 Sanders, Christian Joshua.
Sedimentayao em ecossistemas de mangue: estabilidade,
aplieayoes e estoeagem de carbono em rela<;ao ao nivel do mar /
Christian Joshua Sanders. - Niter6i: [s.n.], 2009.
108 f. :
il ;
30 em.
Tese (Doutorado em Geoquimiea Ambiental). Universidade
Federal Fluminense, 2009. Orientador: Prof. Sambasiva Rao
Patehineelam. Co. Orientador: Prof. Joseph M. Smoak.
CHRISTIAN JOSHUA SANDERS
SEDIMENTA<;AO EM ECOSSISTEMAS DE MANGUE:
ESTABILIDADE, APLICA<;OES E ESTOCAGEM DE
CARBONO EM RELA<;AO AO NivEL DO MAR
Tese apresentada ao Curso de P6s-Graduayao em
Geociencias da Universidade Federal Fluminense, como
requisito parcial para a obtenyao do Grau de Doutor:
Area de
Concentra~ao
Geoquimica Ambiental.
~
PRo:rviRA~INEELAM
0a:::;w
U
PROF
pit
JOSEPH M. (DONNY) SMOAK
CO-ORIENTADOR/UNIV. OF SOUTH FLORIDAIUSA
Q.J~,/C\.-~
~_.0~"'~
PROF. DR. WILSON THADEU VALLE MACHADO
GEOIUFF
NITEROI
2009
Dedicada a minha familha (Luciana, Elizabeth, Chrsitian) que
eu amo muito e me ajudo realizar este trabalho
Estudos sobre a estabilidade de ecossistemas de manguezais localizados ao longo da costa
brasileira foram realizados com base em informayoes sobre as taxas de acumulayao de
sedimentos e relacionando-se estes dados
a
variayao do nivel do mar. Desta forma, investigayoes
na fonte do material organico depositado nestes ecossistemas foram feitas procurando-se
evidencias que pennitam identificar se as florestas sac estaveis ou estao migrando de acordo com
mudanyas no nivel das aguas maritimas. Para realizayao destes estudos, :testemunhos
sedimentares foram coletado em florestas de mangue e em areas intermediarias de planicie de
lama. As coletas dos sedimentos foram feitas nas seguintes regioes: (1) No nordeste, ate a Praia
de Tamandare, Estado do Pemanbuco e (2) No Sudeste, no estado do Rio de Janeiro (3) No suI,
ate Praia de Guaratuba, Estado do Parana .. A taxa de sedimentayao liquida, estimada pela relayao
entre profundidade e idade do sedimento e realizada usando-se
0
210Pbem excesso e confirm ado
par metodos especificos que se baseiam em contaminantes e marcadares naturais. Para
enriquecer a metodologia deste trabalho, radionuclideos vindo do fallout atmosferico 21OPb,7Be,
137Cs, 239
+
240pUforam incluido neste estudo. As variayoes das taxas de sedimentayao nos
ecossistemas de mangue ao longo da costa brasileira aparentemente sac influenciadas pela
relayao entre esta taxa e
0
aumento do uivel do mar. As estratigrafias de TOC/TN, 8-13CcoC),OP,
8
15
Ne series de pigmentos, indicam a fonte do material depositado. Junto com a granulometria,
estas variayoes foram usadas pata mostrar a estabilidade ou migrayao das floresta em areas
especificas. A taxa de sedimentayao nas florestas de mangue varia entre 1,8 e 5,0 mm/ano.
Enquanto na planicie de lanla varia entre 4,0 e 7,3 lrun/ano.
Palavlras chaves· 210
Pb
TOC/TN ()-13
C
()15
N
" , (OC),
i
~
~
..
,.
The stability of mangrove ecosystems in selected regions along the Brazilian coast is assessed
based on investigations of site specific 100 year sediment accumulation rates (SAR) relative to
temporal rise in relative sea leveL Investigations on the sources of the organic matter deposited
in these ecosytems were carried out to interpret if the mangrove forest is stable or migrating.
Addressing this, sediment cores were collected in mangrove forests and intertidal mud flats as far
north as Tamandare, Pemanbuco to Guaratuba, Parana in the South. The net SAR, as estimated
by the age-depth relationships of 21OPb,confirmed by site specific methods such as contaminant
and natural markers. To enrich the methodology of this and future work, atmospheric fallout
radionuclides, 210
Pb
, 7Be, l37Cs, 239
+
240pU, were detected and included in is this study.
Sediment accumulation rates vary along the Brazilian coast, which appear to be influenced by
the relation of this rate to a varying sea level rise. The stratigraphies of TOC/TN, o-13
Cco
C),OP,
Ol5N
and series of pigment results indicate site specific mangal vegetal litter and grain size
variations were used to show stability or migration of the specific forest. Sediment
accumulation rates in the mangrove forests ranged from 1.8 to 5,0 1llm/year, while the 1llud flat
rates were between 4.0 e 7.3 mm/year.
210 . -13 '. 15
Key-words; Pb, TOC/TN, 0 CcoC),o N
FIGURA 1
FIGURA 2
FIGURA 3
, 238
SERlE DE DECAIMENTO DO U 20
i\REA
DE ESTUDO ................................................•..............•.....•......................... 39
LOCAL DE AMOS TRA GEM 40
---------------------------------------------~~
It
;~
~
~
~:i
ill
lit
jii
:d
lf1i
"'illl
ip
AGRADECIMENTOS
LIST A DE TABELAS
LIST A DE FIGURAS
RESUMO
ABSTRACT
1INTR 0 DU~A 0 •.....................................•................................................................................... 11
2 FUND AMENTOS TEO RICA " 18
,
2.1 FUNDAMENTOS PARA 0 usa DE RADIONUCLIDEOS 18
3 0 BJE TIV 0 ; 36
3.1 OBJETIV 0 ESPECIFICOS 36
3.2 HIPOTESE , 37
4 AREAS DE ESTUDO _ _ 38
5 RESULTADOS E DISCUSSOES 41
5.1 ACUMULA<;OES DE SEDIMENTOS RECENTES NA FLORESTA DE MANGUE E
SUA RELEV ANCIA 0 AUMENTO DO NIvEL DO MAR NA ILHA
GRANDE, BRASIL , 41
5.2 TAXA DE ACUMULA<;Ao DE SEDIMENTO EM MA FLORESTA DE
MANGUE E SUA REFERENCIA 0 AUMENTO DO NIvEL DO MAR,
CANANEIA, BRASIL '" 47
5.3 TENDENCIAS NA SEDIMENTA<;AO NAS MARGENS DE MANGUEZAIS,
INFERINDO UM MIGRA<;AO CONTINENTAL DA FLORESTA. 59
5.4 ENTERRAMENTO DE CARBONO ORGANICO VINDO DE UMA FLORESTA DE
MANGUEZAIS E PLANlCIE DE LAMA; SEDlMENTA<;Ao DE 0
AUMENTO NO NIvEL DO MAR 79
6 ESTOCAGEM DE CARBONO EM RELA<;AO AO MYEL DO MAR 97
7 CON CL U
s6
ES 100
8 REFEREN CIAS ~............................•.................................................. 103 '
giubal, vai ser entre 1,8-5,9 mm a-I ate 2100. Mas a projeyao do IPCC
e
referente
a
media do
,
I,
I'
ii',
-------_:
•...
:(
'
.
.
'1 -'..
ib[
1985).
Isto acontece porque cada especie de vegetac;ao que habita
0
mangue vive numa condi<;ao
ecol6gica perto do seu limite de tolerancia. Como os manguezais ocorrem em areas de
po'tt...oo
fl$.f1orestas de mangue reagem a estas mudanc;as (GILMAN et aI., 2007) tem sido encontradas ao
1',1
g~ografica e.g. (LYNCH et aI., 1989; SANDERS et aI., 2008).
E,
portanto, uma escala temporal
nivel do mar sao diferentes da taxa de sedimentayao, podem oeorrer grandes impaetos nos
o Radiois6topo 210Pb, com uma meia vida de 22,3 anos, e urn trayador ideal
para
escala de tempo para se examinar recentes mudanyas climatieas. 210Pb tem provado ser urn
sedimentos, a avaliayao de fluxos de
210
Pb atmosferieos
SaD
tambem necessanas (BASKARAN e
utHilise do 210Pb e do 7Be,
e
necessario ter aces so
as
raz5es de eposiyao destes aeros6is. Estes
GONI, 1997). Isotopos estaveis como &
13
C, &15N e pigmentos podem ser outras ferramentas
Os resultados de este trabalho presente conc1usoes originais e ineditos no Brasil, com a inteny3.o
de contribuir para com as investigayoes internacionais onde existe urn lacuna sobre os assunto
descritos, a seguir;
A variay3.o no aumento do nivel do mar ao longo da costa Brasileira, e a reacaodas
florestas de mangue a estas mudanyas, verificado pelos estratigrafias de OM, TOC, TN,
8
13
C(oc),OP, 8
15
N, pigmentos e granulometriea.
A quantifica93.0 do estoque de carbono nas ecossistemas de mangue no nort!.(de Brasil,
oude os resultados indicam uma migray3.o em direy3.o
0
mar em em poucas quantidades,
relativo a que a media mundial, no sul do Brasit
"
Ii,!
i:~~'
;;11::
!(
II;'!
'I:'
'Iii
:!iii
1[!.11
,;dl
'i::1
fil
~i,::
II",!,
;~:Ij:
.j
i~~;
(KRISHNASWAMI e SEIDEMANN, 1988). Na atmosfera, ele decai si disentigrando, ate
;!1:
'j,:;
chegar ao 21"Pb e posteriormente
ro
2116pb. Os 1\tomos de 21"Ph associarn-se aos aeross6is e siio
:(1
,1.:.:
Ijit
I.!!
'co
i'i!
1i,11
l'\;
],!1i
!
'j~
I
l!j~
I!:'!]
:-!
:j~
~ :--_:.:..:.-....=::~•.•~;
2. FUNDAMENTAc;Ao TEORICA
2.1
FUNDAMENTOS PARA
0
usa DE RADIONUCLlDEOS
se ca1cular taxas de sedimentayao em ambientes diversos. Em particular,
0
210pbse encaixa neste
HARMON,
1992;
RAVICHANDRAN et aI.,
1995). 0
trayador 210Pbpermite a determinayao da
geocronologia dos sedimentos recentes
(~100
anos). A metodologia basica do uso do 210Pbfoi
metodo baseia-se no decaimel1to da serie do 238U(Figura 1). Depois de varios decaimel1tos de
a
226 226 222
e ~, chega-se ao Ra. Com uma r;neia-vida de 1600 arros
0
Ra decai para Rn, urn gas nobre
com uma meia vida de 3,8 dias. Podendo sair,
0
222Rn,de urn ambiente terrestre pelo recuo da
Aproximadamel1te 7,2% dos atomos de 222RI1escapam das rochas/solos graniticas
234Th
CI.
230Th
24,1 d
7,45 x 10
4
a
~
226Ra
1600 a
p
222Ril
3,83 d
~
218pO
214PO
21OPO
1,64 xl0-4
s
3,11 m
138,4 d
2J4Bi
13
P
19,9m
CI.
210Bi
~
5,01d
CI.
214Pb
210Pb
26,8m
206Pb
CI.
22,26 a
CI.
estavel
Figura 1 Serie de decaimento do 238
U
.
Q
pleo da concentrayao de 137Cs em sedimentos acorreu em 1963, epoca em que,
radionuclideo na atmosfera.
0
137CSpode ser usado como urn indice de geocronologia em vanas
metodo dever ser usado com certas restriyoes.
E
necessario urna taxa de sedimentayao constante
SANDERS,
C.l.,
SANTOS, 1., R., SILVA, E., V. AND PATCHINEELAM, S.M. Mercury flux
to estuarine sediments, derived from Pb-210 and Cs-137 Geochronologies (Guaratuba
Bay, Brazil). Marine Pollution Bulletin, v. 52,11.9, 1085-1089,2006.
_"'~P#
.•,.:; D'
ScienceDirect
Mercury flux to estuarine sediments, derived from Pb-210 and Cs-137
geochronologies (Guaratuba Bay, Brazil)
Christian
J.
Sanders
a,*,
Isaac R. Santos
b,
Emmanoel V. Silva-Filho
a
Sambasiva R. Patchineelam
a
~ Departamento de Geoqu[mica, Universidade Federal Fluminetlse, 24020-007 Niter6i-RJ, Brazil
I>
Department of Oceanography, Florida State University. Tallahassee, FL 32306, USA
A sediment core from Guaratuba Bay was used to indicate possible Hg modifications to this coastal environment brought about by
growing agricultural activity. Sedimentation rates were estimated to be 6.\ mm/year and 5.2 mm/year through 210pband 137Csgeochro-
nologies, respectively. Mercury concentrations and organic matter ratios in the surface layers are greater than in the older sediments,
supporting the hypothesis of anthropogenic enrichment. Results show that the Hgflux has raised more than twofold during the second
half of the 20th century. These results point to the need for further studies to substantiate the hypothesis of anthropogenic enrichment
and to quantify point sources of Hg to this estuary.
© 2006 Elsevier Ltd. All rights reserved.
Sediments have the ability to preserve the environmental
history of a drainage basin, and can be useful for making
predictions about how future changes may alter a certain
environment. Alterations in sediment composition may
result from anthropogenic disturbances such as urban
development, road construction, agriculture,' and hydro-
logic changes (Jha et aI., 2003; Smoak and Swarzenski,
2004). Estuaries are preferential environments for sediment
deposition because they are areas of low gradient and may
receive large sediments loads. This makes estuaries interest-
ing sites for studying particle-reactive elements, including
Hg and atmospherically derived radioactive tracers (Iha
et aI., 2003). Many studies have shown that industries, agri-
culture activities, wastewater disposal, gold mining, and the
use of fossil fuels are sources of mercury to the environ-
ment. Its high mobility, organic matter affinity and bio-
• Correspondingauthor. Tel.:+55 2181525508.
E-mail address: zinosanders@yahoo.com
ec.l.
Sanders).
0025-326X/$- seefront matter © 2006ElsevierLtd. Allrightsreserved.
doi:10.1016/j.marpolbu1.2006.06.004
magnification capacity make this element one of the most
harmful metals to biota (Gorski et aI., 2003).
Prominent development in southern Brazil only began in
the 19508. Even though some industries were introduced
during this time period, the most eminent economic activity
has been agriculture. Today, the southern region of Brazil
is highly active in exporting food across the globe. Because
of the steadfast rise in agricultural development during the
second half of the 20th century, studies dealing with local
pollutants as well as sedimentation processes are needed
in this region.
In this paper, we derive 210Pb and 137CSsedimentation
rates and calculate mercury fluxes in a sediment core col-
lected in the landward region of Guaratuba Bay, near the
location of the main freshwater input to the estuary. We
hypothesize that agricultural development during the past
50 years, in particular rice and banana plantations with
subsequent urban impact that includes untreated sewage,
ma.y be disturbing the estuarine environment. Though Hg
was regulated in the 1970s, it is commonly known that
illegal pesticides containing this heavy metal have been
used in Southern Brazil, which may represent a source of
anthropogenic mercury to the estuarine sediments.
Guaratuba Bay (25°52'S; 48°39'W), a seemingly pristine
estuary surrounded by grass plains and mangrove forests,
is situated about 90 miles southeast of the industrialized
city of Curitiba and just south of the busy port of Parana-
gua. It has an area of 48.57 km
2
and is furnished with
freshwater by two main rivers (Cubatao and Sao Joao),
together having an average discharge of approximately
80 m
3
/s (Marone et a!., 2004). Two small fishing towns
are located on opposite sides of the mouth of the estuary
(Fig. I). The development observed in the Guaratuba basin
appears to be a tendency in the region and, therefore, the
results of this study may represent a general pattern along
the south Brazilian coast.
A sediment core, 7 cm in diameter and 40 cm in length,
was collected in Guaratuba Bay (Fig. 1) using an acrylic
tube. The core was sliced in 2 cm intervals until the
10cm depth, 3 cm until the 25 cm depth and 5 cm until
the 45 cm depth. Sampling was done in April 2004, during
low tide. The core was taken in approximately one-meter
water depth. Immediately after extraction, the sediment
showed a dark, uniform color throughout the core. A por-
tion of the original intervals of the core was separated. The
remaining intervals of the sediment core were combined
and sealed in pairs to increase mass, thus decreasing
gamma-ray detecting time. Mercury and physical analyses
were conducted after counting was completed, from the
unfrozen interval pairs.
Gamma-ray measurements were conducted by using a
semi-planar intrinsic germanium high purity coaxial detec-
tor with 40% efficiency, housed in a lead shield and coupled
a multichannel analyzer. Activity was calculated accord-
to well-established methods (Patchineelam and Smoak,
The sedimentation rate was obtained by dividing the
decay constant by the slope of the log-linear plot of
?10
unsupported - Pb versus depth (Appleby and Oldfield,
1992). When a 137Cs peak was discovered, original intervals
of the core were analyzed around the peak area, for the sole
purpose of determining a more precise 137CSgeochronol-
ogy. Depending on activity, samples were counted from
100,000 to 240,000 s.
After gamma-counting was completed, samples were
dried at 50°C. This low temperature was used to avoid
mercury volatilization. Total Hg concentrations were ana~
lyzed by cold vapor atomic absorption spectrophotometry,
following digestion in aqua regia solution and a reduction
with SnCh (Marins et aI., 1998). Standard reference sedi-
ments PACS-2 and NIST SRM-2794 were analyzed in par-
allel with the samples in order to estimate the Hg analytical
recovery. This analysis showed that Hg was adequately
recovered (average of 90
±
6%). Organic matter (OM)
was determined through loss on ignition after combustion
at 450° for 24 h. It was assumed that all the destructed
material was organic matter. Fine sediments (silt and clay)
were determined after wet sieving samples through <63 11m
mesh sieve.
Mercury concentrations ranged between 15 and 44 ng/ g
and showed a general tendency, decreasing with depth.
While fine-grained sediments also increase in surface layers
of the core, organic material (OM) concentrations did not
show any' significant trend in relation to depth (Table 1).
The total 2lOPb activity is depicted by an almost linear
decline in relation to depth, while 226Ra activity is consis-
tent throughout the sediment core (Fig. 2). Due to the dis-
tinct activities of 210Pb and 226
Ra
, 210Pbexis assumed to
.come from the atmosphere or fluxes not explained by the
238Useries equilibrium. The 210Pbexwas fitted to the least
square procedure (r
2
=
0.93; n
=
7;
p
< .05), and the slope
of the log-linear curve
(y
= -
0.05x +
4.40) allowed the cal~
culation of the sedimentation rate (6.1 mm/year) (Appleby
and Oldfield. 1992). Thus, the bottom of the sediment core
(40 cm) was estimated to be near 70 years old. In coherence
with 137Csstudies in other regions of the world, the maxi-
mum activity was assigned as 1963, when atmospheric
nuclear weapons testing reached a peak (Abril, 2003).
The 137Cs peak corresponded to the 21.5 cm depth of
the core (Fig. 3). Given the date of sample collection, a
Table I
Sediment characterization of core
Depth (em)
0-4
4-8
8-13
13-19
19-25
25-35
35-45
Bulk density (g/em
3
)
1.1
1.2
1.1
1.0
1.2
1.2
1.4
Hg (ng/g)
44
36.9
41.2
37.7
32.0
26.9
15.1
<
6311ffi (%)
21.7
11.3
lL2
10.8
5.7
8.2
7.5
OM (%)
9.8
8.8
10.6
10.2
7.9
9.3
5.7
Activity(Bq/kg)
20
10
40 50 60 70
-o-Ra-226
__ Pb-21O
Fig. 2. Profile distribution of total 2lOPb and 226Ra (counting errors are
less than 5%).
Cs-137 (Bqlkg)
2 3
a
')0
~-
.c:
fr
25
A
30
Fig. 3. Profile distribution of
l37CS
(horizontal error bars indicate
counting uncertainties, while vertical error bars indicate date
uncertainties).
sedimentation rate of
5.2
mm/year is implied. This method
shows that the average length of the sediment core
(40
cm)
is approximately
80
years old.
Few other studies have determined sedimentation rates
in similar Brazilian coastal environments, so it is difficult
make comparisons with our data. In the Cananeia-Iguape
Estuary, which receives the drainage of mountainous crys-
talline complex, the 21oPb-derived sedimentation rates ran-
ged between
5.3
and 9.8 nun/year (Saito et aI.,
2001).
In
turn, the sedimentation rates in the highly eutrophicated
2.0
2.5
0
5
10
15
~
:::
E-
20
.c:
fr
25
A
30
35
40
Hg/OM
3.0 3.5 4.G 4.5- 5.0
Fig. 4. Mercury concentrations (ng/g) normalized by organic matter
percentage.
Guanabara Bay (Rio de Janeiro), is as high as
20
mm/year
(Wilken et aI.,
1986).
In the southern region of Brazil, the background concen-
trations of Hg in sediments has been established to be
between
15
and
30
ng/g (Marins et aI.,
2004).
Considering
these figures, Hg concentrations surpassed background
levels near the
25
cm mark. In spite of this enrichment, mer-
cury concentrations are much lower than environments
strongly affected by urban and industtial inputs, such as
Guanabara Bay where mercury in mangrove sediments
may reach
3000
ng/g (Wasserman et aI.,
2002).
The behav-
ior of Hg in coastal sediments may be related not only to
anthropogenic sources, but also to natural characteristics
of-the environment. Mercury distribution may be related
to organic matter content as well (Silva et aI.,
2003).
This
is confirmed by the high correlation observed between
organic matter and mercury
(r
2
=
0.74; n
=
7;
p
< .05),
which could indicate that their source to Guaratuba Bay
sediments are the same. However, when Hg concentrations
normalized by OM are plotted versus depth, a trend
becomes evident (Fig. 4). The Hg/OM ratio steadily
increases in younger sediments, so Hg input is outpacing
the OM load (Benoit et aI.,
1988).
This implies that Hg is
not solely coming from natural sources or from sewage
discharge, supporting the hypothesis of alternative anthro-
pogenic enrichment. The Hg flow was estimated by multi-
plying Hg concentration, bulk density, and sedimentation
rate. Since
210
Pb and 137CSderived sedimentation rates were
similar
(6.1
mm/year and
5.2
mm/year, respectively), we
averaged these rates and used the value of 5.6 mm/year to
calculating the Hg flux into the sedimentary environment.
The slight disparity between sedimentation rate estimates
derived from the 210Pb and
137CS
chronologies may be
due to the fact that
137C
is more mobile, having a lower
K
d
value. From the Hg flux a steady increase for the last
",70
years, going from
12
ng cm-
2
year-
1
to
27
ng cm-
2
1960 1975
Year
year-I, may be seen. This demonstrated a steady increase in
"the Hg flux for the last
rv
70 years, ranging from
12ng cm-
2
year-
J
to 27 ng cm-
2
year-
1
(Fig. 5). This in-
creasing Hg flux may come from various sources, including
direct and indirect effects of agricultural development,
atmospheric deposition and runoff (Mason et aI., 2000).
The direct influence of effluents from industries is unli-
kely because the Guaratuba Bay basin is not industrially
developed. In spite of that, factories located a few hundred
kilometers northward from Guaratuba Bay may be an
atmospheric source of mercury. These activities were regu-
lated in 1979 and from 1980 onward a decrease in indus-
trial uses of Hg was observed in Brazil (Lacerda, 1997).
Being so, if the atmospheric inputs from industries are
the main source of mercury to Guaratuba Bay, one might
expect a reduction in the Hg flux in 1979. Fig. 5 shows no '
reduction in Hg accumulation rates close to the 1979 hori-
zon. The local government does not have reliable informa-
tion about the area of plantations within Guaratuba Bay
basin before 1990s. After that, the area of banana and rice
,plantations has increased steadily
rv
6% per year (agricul-
ture information provided by the Secretaria da Agricul-
tura, Abastecimento do estado do Parana-SEAB).
Taking into account that this development has been the
main environmental change within the basin, it i~the most
probable cause of increasing mercury flow to this estuarine
environment. This is supported by the higher concentra-
tions of fine-grained sediments in surface layers of the core.
Because it may be difficult to tag sources to anthropo-
genic Hg, assumptions have been made, comparing histori-
cal activities with dated Hg concentrations in a sediment
core from Guaratuba Bay. It is known that agricultural
,activity has been steadily increasing beginning from the sec-
half of the 20th century. This growing trend appears to
accompanied by anthropogenic Hg concentrations as
deduced through Hg/OM ratios in the core studied. Fur-
Hg concentrations show a steady rise surpassing
background levels beginning around the 19505. This
trend becomes evident when the Hg flux was calculated~
These results are intended to serve as an indicator ofprevi-'
ously.unknown Hl5.behavioriu a coastal region that is being
expl?Ited for agncultural development. More in~depth'
studIes are needed to conclude point sources of Hg to this
estuary. It is important to point out that any conclusions'
derived from the analysis of a single sediment core may
speculative in characterizing Hg flux to the region.
This work was supported by Conselho Nacionalde
Desenvolvirriento Cientifico e Tecno16gico (CNPq). We
would like to acknowledge the Instituto de Radioprote<;ao
e Dosimetria (IRD) for supplying a certified radionuclide
cocktail that was used for calibrating the gamma ray detec-
tor. We would like to thank the Centro de Estudos do Mar,
Universidade Federal do Parana, for assistance in field-
work. We would also like to thank Luciana Sanders for
laboratory assistance as well as Dr. Wil~on Machado,
Dr. Donny Smoak and an anonymous reviewer for helpful
advice.
Abril, J.M., 2003. Constraints on the use of 137CSas a time-marker
to support CRS and SIT chronologies. Environmental Pollution 129,
31-37.
Appleby, P.G., Oldfield, F., 1992. Application of lead-210 to sedimenta-
tion studies. In: Harmon, S. (Ed.), Uranium Series Disequilibrium:
Application to Earth, Marine and Environmental Science. Oxford
Science Publications, pp. 731-783. .
Benoit, J.M., Gilmour, C.c., Mason, RP., Riedel, G.S., Riedel, G.F.,
1988. Behavior of mercury in the Patuxent River estuary. Biogeo-
chemistry (40), 249-265.
Gorski, P.R., Cleckner, L.B., Hurley, J.P., Sierszen, M.E., Armstrong,
D.E., 2003. Factors affecting enhanced mercury bioaccumulation in
inland lakes of Isle Royale national park, USA. Science of the Total
Environment 1-3 (304), 327-348.
Jha, S.K., Chavan, S.B., Pandit, G.G., Sabasivan, S., 2003. Geochronol-
ogy of Pb and Hg pollution in a coastal marine environment using
global fallout. Journal of Environmt:ntal Radioactivity 69, 145-157.
Lacerda, L.D., \997. Evolution of mercury contamination in Brazil.
Water, Air and Soil Pollution (97), 247-255.
Marins, R.V., Filho, J.P., Maia, R.R., Lacerda, L.D., Marques, W.S.,
2004. Distribuicao de Mercurio Total Como Indicador de Poluicao
Urbana e Industrial Na Costa Brasileira. Quimica Nova 27 (5), 763-
770.
Marins, R.V., Lacerda, L.D., Paraquetti, H.H.M., Paiva, E.C., Villas-
Boas, R.C., 1998. Geochemistry of mercury in sediments of a sub-
tropical Coastal lagoon, Sepituba Bay, Southeastern Brazil. Bulletin of
Environment Contamination and Toxicology 61, 57--64.
Marone, et aI., 2004. Hydrodynamics of Guaratuba Bay - PR, Brazil.
Journal of Coastal Research, Special Issue (39).
Mason, R.P., Lawson, N.M., Sheu, G.R., 2000. Annual and seasonal
trends in mercury deposition in Maryland. Atmospheric Environment
(34), 1691-1701.
Patchineelam, S.R., Smoak, 1.M., 1999. Sediment accumulation rates
along the inner Eastern continental shelf. Geo-Marine 19, 196-201.
Saito, R.T., Figueira, R.C.L., Tessier, M.G., Cunha, 1.1.L., 2001. 210Pb
and 137CS geocbronologies in the Cananeia-Iguape Estuary (Sao
Paulo, Brasil). Journal of Radioanalytical and Nuclear Chemistry 249
(I), 257-261.
Silva, L.F.F., Machado, W., Lisboa Filho, S.D., Lacerda, L.D.,
2003.
Mercury accumulation in sediments of a mangrove ecosystem in SE
BraziL Water, Ail-and-Soil Pollution 1 (145),67-77.
Smoak, J.M., Swarzenski, P.W.,
2004.
Recent increases in sediment and
nutrient accumulation in Bear Lake, Utah/Idaho, USA. Hydrobiology
525, 175-184.
Wasserman, J.C., Amouroux, D., Wasserman, M.A.V., Donard, O.F.X.,
2002.
Mercury speciation in sediments of a tropical coastal environ-
ment. Environmental Techuulogy "
(23), 899-910.
Wilken, R.D., Moreira, I., Rebello, A.,
1986.
210Pb and 137es fluxes in a
sediment· core from Guanabara Bay, Brazil. Science of the Total
Environment
1-2
(58),
195-198.
o
239
Pu e
240pU
tambem podem. ser usados como. urn marcadores, utilizando-se
0
anQ de
:."'-
(ATKINSON e HAWORTH, 1990). Existem Traba1hosdisponlveis na literatura cientificasobre
o
239
Pu e
240
pu como marcadores antropicos, deste estudo esta apresentada em forma de artigo:
SANDERS, C.J.; SMOAK, SANDERS, L. M; WATERS, M. N.; PATCHINEELAM, S:K;
KETTERER, M. E. Intertidal mangrove mudflat
240+
239
pu
signatures, confirming a
210
Pb
geochronology on the southeastern coast of Brazil,
Journal of Radioanalytical and
Nuclear Chemistry,
v. 283, p. 593-596,2010.
J
Radioanal Nucl Chern (2010) 283:593-596
DOl 10.100
7
Is[0967-009-0418-7
.." ,,- < ~
-4
Ii
I
Intertidal mangrove mudflat
240+
239
pU
signatures, confirming
a
210Pb
geochronology on the southeastern coast of Brazil
c.
J.
Sanders'
J.
M. Smoak' L. M. Sanders'
M. N. Waters' S. R. Patchineelam . M. E. Ketterer
Received: 24 September 20091 Published online: 30 December 2009
© Akademiai Kiad6, Budapest, Hungary 2009
Abstract A sediment core was taken to determine if
sediment accumulation rates could be conducted using
240+
239
pu signatures in the coastal mangrove mudflats of
southeastern Brazil. The results from this study show that
240+239pu fallout activities are sufficient und well p~eserved
in the coastal sediments of this region. Sediment accumu-
lation rates determined from the 240+239pU signatures were
4.4 mm/year and 4.1 from 210Pb (CIC) method. A sediment
mixing coefficient rate was calculated using chlorophyll-a
profile (9.5 cm
2
).
The 210Pb dating methods have proven to be an invaluable
tool for recent (~l 00 years) geochemical studies. The
geochronologies derived from excess 210Pb have proven
particularly useful in determining environmental 'impacts
[I].
This is particularly true when this method is supported
C. J. Sanders (121) . S. R. Patchineelam
Departamento de Geoqulmica, Universidade Federal
de Fluminense (UFF), Niteroi, RJ, Brazil
e-mail: zinosanders@yahoo.com
J. M. Smoak· L. M. Sanders
Environmental Science, University of South Florida (USF),
St. Petersburg, FL, USA
M. N. Waters
Natural Scicnces, Shorter College. Rome, GA, USA
M. E. Ketterer
Department of Chemistry and Biochemistry, Northern Arizona
University, Box 5698, Flagstaff, AZ, USA
by other forms of sediment dating (2), Anthropogenic
radionuclides from above-ground Cold War era nuclear
tests are routinely used to confirm and validate 210Pb
results in Northern Hemisphere sediment studies. These
radionuclides, including Pu isotopes, fission products
(
I37
CS, 90sr, 1291)and activation products (3H, 14C), were
deposited globally beginning in the early 1950s from U,S.
and former Soviet Union tests. A 1963/1964 peak of
activity is distinctly recognizable globally as a clll'ono-
stratigraphic marker in sediments, ice cores, and peat
deposits. Stratospheric fallout from nuclear testing has not
been as widely used as a tracer of sedimentation in the
Southern hemisphere; this is due in part to the approxi-
mately fourfold lower inventories of bomb-test fallout [3].
Nevel1heless, several groups have used 137CSand/or Pu as
chronostratigraphic markers in the Southern Hemisphere to
confirm and compliment 210Pb dating models [], 2].
Studies examining 240+239pU deposition along the South
American coastal regions appear to be lacking. Despite this
dearth of 240+239pU studies, Pu would appear to offer
several advantages over 137CS in these environments. In
sediment-water systems, Cs is mainly associated with clay
phases; in saline conditions the
K
d
of Cs is much lower due
to competition with high concentrations of other alkali
cations, and Cs has greater solubility/mobility than is ideal
for a particle-associated sediment marker. Plutonium, on
the other hand, is relatively immobile under both fresh-
water and saltwater conditions, and has been used with
great success in marine sedimentation studies (4). Hence,
we initiated this study to assess the potentia] of 240+239pu
as a sediment chronology tool in intertidal mangrove flats
along the southeastern Brazilian coast. An additional
objective herein is to establish some initial baseline data
against which potential local/regional Pu sources from
reactors or marine transport could be assessed,
Sediment accumulation rates may be altered by the
effects of sediment mixing (i.e., physical and/or biological
mixing), which influences the preservation of the physical
sedimentary structures [5]. For this reason'determining a
mixed region is important in determining geochronlogies
from the 210Pbcx profile. 210Pb has proved to be a valuable
tracer of sediment mixing and accumulation in mangrove
ecosystems [6~8].
In this study, sediment accumulation rates were calcu-
lated using the log profile of 2loPb, which was confirmed
by 240+
239
pu signatures. A mixing coefficient was calcu-
lated based on the chlorophyll-a profile from the equation
provided by Sun et al. [9] and modified by Holmer et al.
[10].
A sediment core (PY3) was collected in a mangrove mud
flat in Paraty (Fig. I), sliced in I cm until the 10 cm and
2 cm intervals until 28 cm depth. Sample aliquots ranging
from 14 to 29 g were dry-ashed at 600 °C for 16 h, and
leached with 50 mL of 16 M HNO). The leaching was
conducted overnight at 80°C with added 242Puyield tracer
(NIST 4334 g, 19 pg). Acid leaching (as opposed to
complete dissolution with HF) is known to solubilize
stratospheric fallout Pu, and there is little possibility that
"refractory" HNOrinsoluble Pu exists in the Brazilian
coastal plain setting. The leachates were diluted to 100 mL,
filtered to remove solids, and the aqueous solutions were
processed with TEY A resin (EIChrom, Lisle, IL) in order
to chemically isolate 3.0 mL Pu fractions in aqueous
ammonium oxalate solution suitabl.e for measurements by
Fig.
1
Study area (Paraty, Rio
de J<lIleiro)located on
Southeastern coast of Brazil.
PY3
refers to the sedimenr core
in this work and indicates study
site
,45' 00'
-23' 00'
sector ICPMS. The chemical procedures followed were
based on those described previously [11], having been
scaled to accommodate larger sample masses. Pu deter-
minations were performed using a YG Axiom MC oper-
ating in the single collector (electron multiplier) mode. The
system was used with a APEX HF desolvating microneb-
ulizer system (ESr Scientific, Omaha, NE) with an uptake
rate of 0.4 mLimin. Qualitative mass spectral scans
(averages of 50 sweeps over the mass range 237.4-242.6)
were collected for selected samples 'prior to the electro-
static sector quantitative scanning of 2)SU, 2)9pu, 240pU,
and 242PU. Sufficient Pu was recovered, and the decon-
tamination of Th and U was excellent. Detection limits
were evaluated based upon the analysis of two blanks and
considerations regarding the obtained mass spectra. A
detection limit of 0.0
I
Bq/kg of 239+240pU is applicable for
samples of nominal 25 g mass. ~.
Sediment accumulation rates using the 210Pb method for
the core were determined by the depth-age relationship of
the unsupported 210Pb profile. Splits of the core sections
were sealed in 70 mL petri-dishes for at least 3 weeks, to
establish secular equilibrium between 226Ra and 214Pb.
Gamma-ray measurements were conducted by using a
semi-planar intrinsic germanium high purity coaxial
detector with 40% efficiency, housed in a lead shield,
coupled to a multichannel analyzer. The 210Pb activity was
determined by the direct measurement of 46.5 keY pho-
topeak, while 216Ra activity was calculated using the proxy
214Pb (351.9 keY) [12]. Activities were calculated by
multiplying the counts per minute for each radionuclide,
minus background counts, by a factor that includes the
gumma-my intensity and detector efficiency. This factor
was determined from standard calibrations using an
-44' 00'
,23' 00'
-44'
15'
km
/"'Fl'l'R"'\
o
5 10
Table 1
Paraty mangrove core (uncertainties are ± one SD for n
=
3
measurements) depth midpoint 239+
240
pU (Bq/kg) 240pu/239
PU
atom
ratio
0.191 ± O.OOS"
0.124 ± 0.010
0.113±0.009
0.135 ± 0.024
0.140
±
0.009
0.122 ± 0.006
0.120 ± 0.007
0.121 ± 0.003
0.127 ± 0.002
0.103 ± 0.009
0.039 ± 0.002
0.046 ± 0.004
<0.02
<0.02
0.21 ± 0.03"
6.20 ± 0.05
0.20 ± 0.01
0.20 ± 0.07
0.20 ± 0.03
0.19 ± 0.04
0.19 ± 0.01
0.17 ± 0.01
0.17 ± 0.01
0.19 ± 0.02
Could not be reliably measured
h
Could not be reliably measured
" Uncertainties are
±
1 SD
(II
= 3)
b
The ion count rate for 2"U
pU
is insufficient to perform ratio mea-
surements, although Pu activity is detected
efficiency curve obtained by measuring and analyzing a
certified standard cocktail of radionuclides. The excess
210Pb ("I°Pb
ccx
)) acti vi ty was esti mated by subtracti ng the
226Ra from the total 210Pb activity. Samples were counted
for 86.000 s in identical geometrical cylinders. Self-
absorption corrections were calculated following (13). The
sedimentation rate was obtained through the Constant Ini-
tial Concentration (CIC) approach outlined by Appleby and
Oldfield (14). ChlorophylI-a was measured using an HPLC
system following the methods of Lyavitt and Hodgson (15)
designed particularly for sedimentary pigments.
The core intervals at 24-26 and 26-28 cm contain no
detectable 239+
240
pU (Table I). Plutonium is first detected
in the 22-24 cm interval (0.046
±
0.004 Bq/kg 2.W+240pU)
and is also detected in all overlying layers up to the surface,
There is no consistent activity pattern that resembles the
expected atillospheric deposition history, or the patterns
expected in quiescent freshwater lakes such as Loch Ness
(11). Instead, the 2.19+240pUactivity is relatively uniform in
'. all core intervals from 0 to 2 cm through 18 to 20 cm.
Therefore, it is not possible to assess a
1963
peak deposi-
tion date from this profile. The Pu profile reveals that there
is a complex depositional environment with disturbances,
bio-turbation, resuspension, or erosion all at work. One can
say with certainty that the material below 24 cm
;:'was deposited pre-bomb (that is, prior to the early 1950s).
3.5
+
3.0
•
.
.
7-
'"
2.5
+
0
....
~
2.0
.Q
I:l..
Z
1.5
...l
1.0
0.5
0 5
10 15 20
Depth
(em)
Fig. 2
Log
linear profile of the unsupported 211lPb vs, depth of th'e .
sediment core of this work (PY3)
This affixes an upper limit on the sedimentation accumu-
lation rate (SAR) to be near
4.4
cm/year. The Pu atom ratio
data indicate that the Pu is originating from stratospheric
fallout. These results are c0!"!sistent with the 240ptfl239pu of
0.180 ± 0.014 discussed by Kelley et al. (3).
The mangrove core 210Pbcx profile is almost homoge'-
neous until ~
6.5
cm depth. Below this apparent mixed
region, activity generally decreases with depth. The net
downcore decrease in the 2IoPb(cx) activity may be seen in
the core profile shown in Fig. 2, allowing a direct mea-
surement of the 210Pb(CX) log profile below the mixed
region. The almost linearly decrease in the 210Pbtcx) implies
a consistent rate of sedimentation
[14],
Following the
procedure outlined by the 210Pb (eIC) dating method, a
Table 2 Dry bulk density (g/C~3) and total chlorophyJl-a profile
(llg/cm
3
)
Depth (em) DBD (g/cm')
Chl-a
(Ilg/cm')
I
0,14
6.08
2 0.14
5.06
3 0.17 4.96
4
0.16
2.S0
5
0.15
3.05
6 0.18
3.07
7 0.18
1.89
S
0,19
I.S6
9
0.19
I.S4
10
0.24 3.29
12 0.18
2.94
14
O,IS
1.25
16
0.17
0.87
IS
0.14
0.42
20
0.16 0.14
22 0.13 0.21
24 0.11 0.07
26 0.12 0.14
28 0.11
0.06
~.;-
<f.:)
Springer
geochronology of the core was established. The statistics
related to the 2loPb(cx) distribution are on figures and as
follows; (R
2
=
0.71, n
=
13; p
<
0.05) from the 6.5 cm
depth to the bottom of the core, giving SAI\ of 4.1 mm/year.
Since the entire core was comprised at least 95% mud by
content
«63
~lmsize fraction), grain size normalization was
not needed [16].
The chlorophyll-a and dry bulk density profiles are
shown in Table 2. A mixing coefficient was calculated
through these data [9, 10], yielded a mixing rate of
9.5 cm
2
/year. This rate is slightly lower than the one found
by Smoak and Patchineelam
[7],
who found significant
physical and/or bioturbation. Typical continental shelf
margin environment have mixing rates ranging from
1
to
30 cm
2
/year [17, 18].
The detection of a recognizable 239+
240
pU
sediment profile
in this southern Brazilian coastal environment is promising
in terms of future uses of plutonium chronology in the
Southern Hemisphere. There is a paucity of data for bomb-
test radionuclides such as Pu and 137Cs in the Southern
Hemisphere, in part because of approximately fourfold
lower inventories of fallout [3, 19]. Plutonium probably
presents more potential in Southern Hemisphere studies
because, unlike 137Cs (t1/2
=
30 years), it is not signifi-
cantly decaying; Pu is better suited geochemically for
brackish and salt water conditions, and as we have dem-
onstrated, Pu is effectively analyzed by rapid mass spec-
trometric methods. We expect that Pu offers a great deal of
potential for examining sedimentation processes with
large-scale data generation.
Both the 2.19+
240
pU
and 210
Pbcx
profiles reveal non-ideal
behavior in terms of applying conventional dating models;
nevertheless, both sets of radionuclide data generate
approximate SARs in good agreement (4.4 and 4.1 c'm/year,
respectively). This is not unexpected, given the complex
depositional characteristics and mixing rates present in the
mangrove mudAat. Geomarkers such as Pu and 210Pb are
invaluable for scientific studies dealing with topics that
range from climate change models [6] to formulating pol-
lution records in mangrove ecosystems [I].
Acknowledgments This work was funded by the Conselho Nac-
jonal de Oesenvolvill1ento Cientifico e Tecnologico (CNPq), Brazil
and Fulbright support to J.M.S. M.E.K. acknowledges support for
ICPMS instrtlll1entalion from the US National Science Foundation
(CHE-O I 16804 ancl EAR-0450977).
I. Sanders CJ, Santos IR, Silva EY, Patchineelam SR (2006) Mar
Pollut Bull 52: I089
2. Saito RT, Figueira RCL, Tessier MG, Cunha IlL (200 I) Radio-
anal Nucl Chem 249:251
3. Kelley JM, Bond LA, Beasley TM (1999) Sci Total Environ
237/238:483
4. Zheng J, Yamada M (2004) Environ Sci Tech 38:3498
5. Nittrouer CA, Sternberg RW (1981) Mar Geol 42:201':1
6. Sanders CJ, Smoak JM, Naidu AS, Patchineelam SR (2008)
J Coastal Res 24:536
7. Smoak JM, Patchineelam SR (1999) Mangroves Salt Marshes
3: 17
8. Lynch CJ. Meriwether JR, McKee BA, Vera-Herrera F, Twilley
RR (1989) Estuaries 12:284
9. Sun M, Aller R, Lee C (1991) J Mar Res 49:379
10. Holmer M (1999) Estuarine Coastal Shelf Sci 48:383
II. Ketterer ME, Hafer KM, Jones YJ, Appleby PG (2004) Sci Total
Environ 322:221
12. Appleby PG. Nolan PJ, Oldfield F, Richardson N, Higgitt SR
(1988) Sci Total Environ 68: 157
13. Cutshall NI-l, Larsen IL, Olsen CR (1982) NliC Inst Meth 206:309
14. Appleby PG. Oldfield F (1992) In: Ivanovich M, Harmon S (eds)
Uranium series disequilibrium: application to eal1h, marine and
environmental Science. Oxford Science Publications, London,
pp 731-783
15. Leavitt PR, Hodgson OA (200 I) In: Smol JP, Birks HJP, Last
WM (eds) Tracking environmental change using lake sediments,
terrestrial, algal, and siliceous indicators, vol 3. Kluwer Aca-
demic Publishers, Oordrecht, the Netherlands, pp 295-325
16. Ravichandran M, Baskaran M, Santshi P, Bianchi T (1995) Chem
Geo] 125:291·
17. Carpenter R, Peterson ML, Bennett
IT,
Somayajl1ll1 BLK (1984)
Geochim Cosmochim Acta 48: 1949 .
18. OeM aster OJ. McKee BA, Nittrouer CA, Jiangchl1 Q, Guodong C
(1985) Cont Shelf Res 4: 143
19. Godoy JM, Carvalho ZL, Fernandes. FC, Oanelon OM, Ferreira
ACM. Roldao LA (2003) J Environ Radioactivity 70: 193
.:\
2008.). Conhecendo-se 0 passado do local e os fatores de enriquecimento, conclusoes podem ser
de
0
parente (i.e., 234
Th
de 238
U
, e 210Pb de 222Rn depois de uma sene de decaimento), ii)
deposiv3.o atmosferica direta (fall out de 210Pb e 7Be), eros3.o seccional do fluxo pela descarga de
como indicadores do material orgamco em sedimentos
e
comum em estudos geoqufrnjcQ~/
material orgamco em sistemas de mangue. Estes registros SaDimportantes na interpretac;ao·das··
1999).
E
COllum ver as concentrac;oes do
MO
levement~ mais alto na superficie em florestas
de
dnistica na composiyao elementar molecular e isot6pica da MO (MEYERS, 1994), sendo que
0··
da floresta de manguezal 0 enriquecimento de
OC
I3
(OC) nas mais baixas profundidades:
minerolizado C02 em BC, enquanto os produtos de degradayao sao enriquecido em BC
2006). Isso
e
menos significante em areas inundadas mais frequentemente e com maior durayao
:;".
concentrayoes de MO, favorecendo a fracionamento pelas plantas que seletivamente escolhe 14N,
acrescentando
15
N no sedimento e tendo valores mais baixo de
(5
15
N (MAZUKA e SHUNULA,
Existem poxies de
OBC(OC)
e
015
N estabelecidos para arvores terrestres, especificamente
do m<;l.nguezal,especificamente quando
0 ()
13
C(OC)
e
plotando contra
0
OC/1N. Estes
podem indicar a origem da deposiy8.o do MO (MEYERS, 2003) especificamente em
manguezais (BOUILLONet aI., 2003; BOUILLON et aI., 2004; LALLIER-VERGES
1998)
Os
testemunhos foram coletados em varias areas de manguezais que foram escolhidos por
representar ambientes tipicos de ecossistemas Brasileiros, incluindo Guaratuba, Parana (8 25
50.085 e W 48 39.787); Paranagua, Parana (8 25 18.387 e W 48 23.570); Ilha Grande, Rio de
.
-
Janeiro (8 23 10.7 e W 44 17.2); Paraty, Rio de Janeiro (S 23 14.983 e W 4441.965) Cananeia,
Sao Paulo (8 25 05'45 e
W
4759'41) e Tamandare, Pernambuco (8 08 40.050 e W 3506.167).
A
Figura 3 mostra os tres locais de amostragem nas areas de estudo: 1) Panicie de lama, 2) margin,
3) f10resta
'"
.-Kparaty, Rio de Janeiro
\ Ilha Grande,Rio de Janeiro
Cananeia,Sao Paulo
Paranagua, Parana
,
Figura 2 Areas de estudo
~vlangroveforest
H~~_~~~ _
Low
tide
3~
;::~
para atingir
0
objetivo desta tese, abordando a hip6tese. Estes sub-topicos esrno apresentado em
5.1 ACUMULA<;OES DE SEDIMENTOS RECENTES NA FLORESTA DE MANGUE E SUA
RELEV ANCIA 0 AUMENTO DO NIvEL DO MAR NA ILHA GRANDE, BRASIL
013C(OC),
e
o15
N indica urn. constante [onte de detrito de acumulayao vegetal, dominado peIo
Recent Sediment Accumulation in a Mangrove Forest and Its
Relevance to Local Sea-Level Rise (Ilha Grande, Brazil)
tUniversidade Federal de Fluminense
(UFF)
Departamento de Geoquimica
Niter6i-RJ, Brazil, 24020
zinosanders@yahoo.com
tUniversity of South Florida
Environmental Science
St. Petersburg, FL 33701, U.S.A.
iUniversity of Alaska Fairbanks
Institute of Marine Sciences
Fairbanks, AK 99775, U.S.A.
SANDERS,C.J.; SMOAK,J.M.; NAJDU,
A.B.,
and PATCHINEELAM,S.R., 2008. Recent sediment accumulation in
a :mangrovefore~t.3.ndits relevance to local sea-level rise (Ilha Grande, Brazil).
Journal of Coastal<Research, 24(2),
533-536. West Palm Beach (Florida), ISSN 0749-0208. .
,tll!l"'I:.
!~
~.
~
~
An accumulation rate in a well-developedmangrove forest has been associated with relative sea-levelrise on an island
off the coast of Rio de Janeiro State. This rate was calculated by 210Pbdating models from a single sediment core.
Results indicate an accumulation rate ofapproximately 1.7
mmJy
for the past approximately 100 years. This rate is
almost identical to the ongoingeustatic mean rise in globalsea level,indicating a tectonically stable mangrovehabitat.
Organic C (OC),total N, 8
13
C(oc),and Sl5Nvalues from selected core intervals suggest a constant source of accumu-
lating vegetal debris, dominated by C3-typevegetation with insignificant input ofmarine-derived organic matter, and
a stable subaerial mangal habitat.
A significant sea-level rise (SLR) has the potential to in-
undate low-lying coastal areas and thus adversely affect the
human population and man-made structures in these areas.
The Intergovemmental Panel on Climate Change OPCC,
2007) has concluded that the global sea-level rise (GSLR) will
be 1.8-5.9 mm/y by 2100 because of global warming. The
IPCC projection refers to mean GSLR and does not predict
local sea-level rises. Large variations in relative Sea level
(R,SL)are found along the coastal regions of the world (PILK-
EYand COOPER,2004). Examining local sea-Ievel"oscillations
over the past 100 years and comparing them to the eustatic
rates will provide means to develop models to predict local
changes over the next century. Many parts of the world have
site-specific tide level data ii'om which to make these com-
parisons. However, in the south Atlantic, especially along the
7500-km Brazilian coast, few tide-gauging stations are in
place with duration sufficient to detect patterns of sea-level
changes during the past century (BLASCO, SAENGER, and
JANDOET,
1996).
Sediment accumulation rates (SAR) in mangrove forests
can be used to estimate RSL rates during the past 100 years
DOl:
10.2112/07-0872.1 received
14
May 2007; accepted in revision
24 August 2007.
(LYNCH
et aI.,
1989; SMOAKand PATCHINEELAM,1999) as
well as sea-level variations of longer term (WooDRm'FE,
THOM,and CHAPELL,1985). Because mangals thrive in geo-
graphically limited coastal locations, minimal variation in
their hydrological regime can cause their mortality or migra-
tion (BLASCO,SAENGER,and JANDOET, 1996). The survival
of this sensitive ecosystem depends on the quasi-equilibrium
between SAR and local sea-level oscillations, in that wetlands
have the potential to vertically accrete in pace with the SLR
(LYNCH
et al.,
1989; NYMAN
et aI.,
2006). Therefore, under-
standing of the depositional and tectonic regimes in conjunc-
tion with the local SLR has practical use to elucidate histor-
ical changes of the mangal habitat (BLASCO,SAENGER,and
JANDOET, 1996; HASLETT
et al., 2003).
Ilha Grande, an island on the southeastern coast of Brazil,
is located about 100 !un southwest of Brazil's second most
populated city, Rio de Janeiro. It is 193 km
2
in area, made
up of sloping mountains, with its highest point at 1031 m.
The sediment core was collected in a well-protected site, with-
in an inlet and behind a barrier island, on the Atlantic side.
This is one of the few areas on the island that is oflow gra-
dient and isolated enough to support a well-developed man-
grove forest. The study site is located in a biological reserve
(Figure 1, dotted gray line) and marine park (dotted black
line), in which public access is not permitted.
ll<Q.\'4
. ";;'1 ~
q,j
Ii
In this paper, we report a case study in which the sedi-
mentation rate on the mangal forest was determined by the
210Pbmethod, which is an ideal tracer for determining sedi-
ment accumulation rate on a loo-year timescale, and exam-
ining possible perturbations on the mangal environment con-
sequent to the predicted rise in sea level from global warm-
ing. Stratigraphic variations in the carbon and nitrogen iso-
topes (6'3C and SIGN)and the carbon-to-nitrogen ratios
(CIN)
were examined to infer the source of organic matter to the
mangal substrate and, from this knowledge, to deduce man-
grove habitat stability during the past century.
A sediment core was collected in 2005 from a site at
25°18.40'8, 48°23.70'W, about 10 m inland on the seaward
side of the mang:rove fringe, by inserting a 7-cm-diam plastic
tube into the substTate during low tide. The sediment was
ext:ruded out of the tube and sectioned at l-cm intervals from
the core top to 10 em and at 2-cm intervals in the residual
34-crn core. Approximately a 5-15split of selected sections was
acidified to remove carbonate, dried, and powdered, and a
portion was taken for analyses of organic carbon (OC), nitro-
gen (N), /)13C,and Sl5N with an isotope ratio mass spectrom-
eter (Thermo Finnigan Model Delta Plus XP) according to the
method ofNAIDU
et al.
(2000). Organic matter (OM) was de-
termined as OC
X
1.8 (TRASK,1938). From the original wet
section, a split was taken for determining its mass, which was
estimated by taking into consideration the split's porosity on
the basis of fractional water content and assuming densities
of the interstitial water and· sediment as 1.0 and
2.5.,
g.(cm;',
respectively. Fine sediment content (silt and clay) was ob-
tained by wet sieving through a 63-fLm mesh screen (FOLK,
1968).
For radionuclide analyses, the remaining sediments at
each interval were sealed for at least 3 weeks to establish
secular equilibrium between 226Raand 214Pbin 7o-ml petri
dishes. Gamma ray measurements were conducted with the
use of a semiplanar intrinsic germanium high-purity coaxial
detector with 40% efficiency, housed in a lead shield and cou-
pled to a multichannel analyzer. Lead-21O activity was de-
termined by the direct measurement of the 46.5-KeV gamma
peak, whereas 226Raactivity was calculated from 214Pb(351.9
KeV) (APPLEBY
et al.,
1988). Activities were calculated by
multiplying the counts per minute for each radionuclide mi-
nus background counts by a factor that includes the gamma
ray intensity and detector efficiency. This factor was deter-
mined from standard calibrations with an efficiency curve ob-
tained by measw'ing and analyzing a certified ~tandard cock-
tail of radionuclides; this stantiard was certified by IRD
(C/87/AOO,
Instituto de Radioproter;ao e Dosimetria). The ex-
cess 210Pb (21°Pb
cex
»
activity was estimated by subtracting
226Ra from total 210Pb activity. Samples were counted for
120,000 seconds in identical geometrical cylinders. This
counting time was predetennined to be adequate for obtain-
ing the desired radionuclides with relatively low errors
(Sanders et al., 2006). Self-absorption corrections were cal-
culated following CUTSHALL,LARSEN, and OLSEN (1983).
The sedimentation rate was obtained through the constant
rate of supply (CRS) and constant initial concentration (CIC)
dating methods (APPLEBY and OLDFIELD, 1992). Sample
depth intervals were normalized by the average dry bulk den-
sity of the bottom five samples according to LYNCH
et al.
(1989). This was done to account for organic material com-
paction that is characteristic of mangrove sediments (CA-
I-lOONand LYNCH,1997).
We address two aspects of our investigations on the mangal
forest: the stability of the mangrove forest habitat and the
sediment· accumulation rate in the forest in the context of
SLR.
The OC, total nitrogen (TN), 3
13
C
IOC
),
and /)15Nvalues (Ta-
ble 1), having standard deviations of 5.8, 7.2, 1.6, and 4.5,
respectively, show small variations relative to depth. Mi-
crobe-mediated remineralization of OM could result in small
changes in the isotopic compositions. Sediment OM is a mix-
ture of different types of organic compounds, each with spe-
cific isotopic compositions. The proportions of these com-
pounds could change during early diagenesis and, thus, alter
the isotopic values of the residual OM (LEHMANN
et al.,
2002). The o15Ndata show a relatively higher value in the
upper core layer, attended by lower values in the lower ho-
rizons, which could be attributed to oxic conditions in the core
top and anoxic potential at the core bottom (LEHMANN
et al.,
2002). The relatively low /)13C
COC
)
and 1j15Nare typical values
Corrected - .
Dl:Y
Bulk
Sediment
(%)
Depth (em)
Depth (em)
Density (glem') Porosity
(%)
<63
fill
2I.Opb(lll')
(Bq/kg)
0-1
0-0.89
1.20
51.87
7.69
21.48 :': 1.85
1-2
0.89-1.73
1.14
54.17 22.58
21.66 :': 2.34
2-3
1.73-2.50
1.04
::\
57.63 12.50
22.67 :': 2.60
3-4
2.50-3.18 0.91 63.09 10.53 45.66 :': 4•.91
4-5 3.18-3.89
0.97 60.94
28.57 46.15
±
5.20
5-6
3.89-4.83
1.27
48.72 18.75
13.09 :': 1.32
6-7 4.83-5.83
1.34
45.86
11.76
8.31 :': 0.97
7-8 5.83-6.57
1.00
59.31 4.55
12.76 :': 1.55
8-9
6.57-7.35
1.06
57.22 7.32
9.74:': 1.28
9-10,
7.35-8.29
1.27 48.48
3.57
5.84 :': 0.64
10-12 8.29-10.04
1.18
51.64
21.05
4.95 :': 0.55
12-14
10.04-11.55
1.02
59.05
11.11
5.22 :': 0.63
14-16
11.55-12.94
0.93 62.22
31.03
6.88 :': 0.71
16-18
12.94-14.06
0.76
69.40
8.33
13.56 :': 1.47
18-20 14.06-15.33 0.86
65.50 20.00
11.49 :': 1.23
20-22 15.33-16.56 0.83
66.77 25.81
5.91 :': 0.71
22-24 16.56-17.68
0.75 69.55 17.65
6.27 :': 1.01
24-26
17.68-18.98 0.88
64.61 14.29
1.82 :': 0.30
26-28 18.98-20.45
0.99 59.91 18.52
0.80 :': 0.11
28-30
20.45-22.41
1.32
46.29 13.89
0.54 :': 0.07
30-32
22.41-24.65
1.52
38.57 10.26
0.19 :': 0.03
32-34 24.65-26.66
1.35
44.68
6.67
0.55 :': 0.07
34-36
26.66-28.98
1.57
36.89
8.16
0.64 :': 0.10
relating to terrestrial OM sources, most likely the mangrove
forest, with insignificant admixture of marine-derived OM
(BOUILLON
et al.,
2003, 2004; LALLIER-VERGES
et al., 1998;
MAZUKAand SHUNULA,2006; NAIDU
et al.,
2000, and refer-
ences therein; WOOLLER
et al.,
2003). This database suggests
that the habitat of the mangal forest has been quite stable
and subaerial during the past approximately 100 years. In-
deed, when the 8
13
C(oc)values are plotted against the OC/N
data, the scatter plots lie in a cluster that is attributed to C3
(MEYERS,2003), mangrove vegetal sources (BOUILLON
et al.,
2003, 2004; LALLIER-VERGES
et a.l., 1998).
The close ranges of OC and TN in the core represent an
overall constant depositional flux of organic matter. Indeed,
the lack of a grain size trend (Table 1) is a sign that the
runoffltransport of sediment regiine has not changed signifi-
cantly over the time interval of the core, further evidencing
a consistent source of the sediment load
(e.g.,
COHEN, BEHL-
ING, and LARA,2005).
The 21oPb
rcx
)profile shows a subsurface peak at the 3.5-cm
mark of the sediment profile (Table 1), which could indicate
that the core has been affected by physical mixing, biotur-
bation, or both, either of which could allow the direct trans-
port of fine organic-rich, relatively high activity material to
depth, decaying organic material, or both. The three condi-
tions above might be associated with this relatively low
21Opb,ex)activity in the superficial deposits (ApPLEBY and
OLDFIELD,1992), to an increase in recent sediment load, or
to both. Below 3.5 cm, the core indicates a net decreasing
trend in the 21opb,ex)activity with depth, until approaching
background levels (Table 1). Neither porosity nor fine sedi-
ment «63 f.Lm~concentrations appear to be an influencing
factor in the 21°Pb<ox)distribution because they are relatively
homogeneous throughout the core (Table 1). Under these cir-
cumstances, a direct sedimentation rate might be gathered
from the 21Opb'ex)profile. The CRS approach was one of the
dating models chosen to calculate the SAR because the
210Pb<ex)profile is not completely linear. The CRS model takes
into account variations in sedimentation and is not affected
by the relatively depressed activity in the superficial layers
(ApPLEBYand OLDFIELD,1983). The other SAR method used
in this study was Cle, in which the slope of the log-linear
curve
(y
=
-0.17x
+
3.85) was used that excludes the apc
parently altered superficial layers
(r
2
=
0.78;
n
=
20;
p
<
0.05). The 8AR in this core was determined to be approxi-
mately 1.6 and 1.8 mm/y with the CRS and CIC models, re-
spectively. This result is comparable to that of SMOAKand
PATCHINEELAM(1999), who found a SAR of 1.2 mm/y in a
mangrove forest in nearby Sepitiba Bay. These rates are also·
in agreement with estimates of the global mean SLR of 1.7
±
0.3 mm/y taken from tide gauge records from 1870 to 1992
(WCRP, 2006) and from PIRAZZOLI(1986) who reported a 1.5
mm/y SLR rise over the previous century. From this, the SLR
for the last approximately 100 years in this area is most like-
ly associated with a eustatic rise and not tectonic factors.
Therefore, we assume that eustatic factors are the controlling
force in the SLR to the area and that global models might
apply in determining current and future rates.
The SAR taken from a single sediment core in an llha
Grande, Brazil, mangrove forest has been approximately 1.7
mm/y during the previous century, calculated by averaging
the CRS and CIC dating models. This rate is in agreement
with an estimate indicating regional RSL and with work pre-
sented on the GSLR. Organic carbon, total nitrogen, 013C,OC)'
and o'5N data were used to verify the stability of the forest
habitat, indicating that mangrove migration did not occur
and that the sediment load has remained constant during the
past approxi...m"tely 100 years. Because the SAR is almost
identical to the eustatic SLR, any progressive rise in the sea
level, consequent to increasing global warming, could ad-
versely affect this region. Such a disaster could happen if the
trend of the past
10
years is sustained in acceleration in the
rate of sea-level rise to 3.2 :2: 0.4
mmig,
as indicated by the
TopexIPoseidon and Jason Satellite altimetry radar measure-
ments (http://sealevel.colorado.edu, as cited in MOTYKA et al.,
2006;
NEREM,
2005).
Because the RSL will vary fi'om one area to another, the
intention of tlus paper is to contribute to a better understand-
ing of the effect of rising sea level near the highly populated
city of Rio de Janeiro. The use of SAR in mangrove forests as
a proxy for past sea-level variations will aid in understanding
the effect of an accelerating SLR This RSL-mangrove sedi-
mentation relationship could be applied over as much as two-
thirds of the Brazilian coast, which, for the most part, is de-
ficient in recent SLR data. In addition, tlus approach would
be useful in many tropical areas, in that approximately 75%
of the ·....arld's coastline between latitudes 25°N and 25°S are
dominated by mangrove forests.
We would like to aclmowledge the Instituto de Radiopro-
tecao e Dosimetria (IRD) for supplying a certified radionu-
elide cocktail used to calibrate the gamma ray detector and
Luciana Sanders for help in laboratory and field work. This
work was funded by the Conselho Nacional de Desenvolvi-
mento Cientitico e Tecnol6gico (CNPq), Brazil, and Fulbright
support to J.M.S.
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5.2 TAXA DE ACUMULA<;AO DE SEDIMENTO EM MA FLORESTA DE MANGUE ESUA
REFERENCIA 0 AUMENTO DO NIvEL DO MAR, CANANEIA, BRASlL - .
de sedimentav3.o foi estimado pelo relavao entre a data e a profundidade basiado no 210Pb e
no
137
Cs que foi entre 2.5 and 3.9 mm ano·
I
• Estas taxas foram companivel os estimativos
$.1
local (4 mm ano·
I
)
indiacdo pelo maragrafo na area, e mais alto do que media mundial do
aumento no mvel do mar (1.7
±
0.3
mm ano·
I
).
Os strategrofias do TOC/TN, 8-
13
C
c
oC), OP e
SANDERS, C.J.; SMOAK, J.M.; NAIDU, A.S.; PATCHINEELAM, S.R. Mangrove forest
sedimentation and its reference to sea level rise, Cananeia, Brazil. Environmental Earth
Sciences, D.O.!. 1O.1007/sl2665-009-0269-0, pp. 12 inpress.
Mangrove forest sediInentation and its reference to sea level rise,
Cananeia, Brazil
Environ Eatth Sci
DOl Ia.! 007/s 12665-009-0269-0
Christian J. Sanders' Joseph M. Smoak'
A. Sathy Naidu . Denise R. Amripe .
Lucian M. Sanders' Sambasiva R. Patchineelam
Received; 18 March 2009/ Accepted: 29 July 2009
©
Springer- Vcrlag 2009
Abstract The stability of a mangrove ecosystem in
Cananeia, Brazil, is assessed based on investigations of the
site-specific temporal rise in relative sea level during the
past 50 years,
I
DO-year sediment accumulation rates (SAR)
and sources of organic matter (OM). Addressing this, three
sediment cores were collected in a transect,intel1idal mud
flat, mangrove margin and well into the forest. The net
SAR, as estimated by the age-depth relationships of
210
Pb
and 137Cs, is between 2.5 and 3.9 mm year-t. These rates
are comparable to the estimates based on the Pb and Zn
contaminant markers corresponding to mining initiation in
the region in 1918. Further, the SARs are lower than the
rate of regional relative sea level rise (4 mm year-I) as
indicated by the past 50-year tide gauge record, but the rate
is higher than the eustatic sea level rise (1.7
±
0.3 mill year-I). The stratigraphi'es of TOC/TN,
(5
13
C
tOC
).
OP and b
l5
N indicate site-specific mangal vegetal litter,
which is the predominant source of OM at all core sites,
during the past century and reflects a stable mangal system
over that time span.
C.
J. Sanders
(181) .
S. R. Parchineelam
Departamento de GeoCjuimica, Universidade Federal de
Fluminense (UFF), NiterDi, RJ, Brazil
e-mail;zinosanders@yahoo.com
1. M. Smoak· L. M. Sanders
Environmental Science, University of South Florida CUSF),
St. Petersburg, FL, USA
A. S. Nuiclu
Institute of Marine Science, University of Alaska Fairbanks
(UAF), Fairbanks, AK, USA
D. R. Araripe
Departamento de Qufmica Analftica, Universidade Federal de
Fluminense CUFF), Nireroi, RJ, Brazil
Keywords ~IOPb . 137 Cs . Trace metal contamination .
TOC . TN . OP .
b
I3
C(OC) .
b!5N
The relation between global warming and sea level rise
(SLR) is an important issue worldwide (Hansen et al. 2005;
Meehl et al. 2(05). The Intergovernmental Panel on Cli-
mate Change (IPCC 2(07) has projected that the rate of
global sea level rise (GSLR), consequent to global warnl-
ing, will be 1.8-5.9 mm ~ear-I by 2100. However, the
IPCC projeclion refers to mean GSLR and does not apply
to local or regional sea level changes.
Along the 7,500 km coast of Brazil, little is known
about the relative sea level rates (RSL) or how a SLR might
affect its coastal region. This is because, unlike matl'y
countries in the northern hemisphere, tide gauges have not
been utilized consistently in South America. Tide gauge
records are useful because they have provided trends in
local sea level changes, pal1icularly dUling the past century
(Blasco et al. 1996). As large variations in RSL rates are
found along the coastal regions of the world (Pi key and
Cooper 20(4), examining local sea level oscillations over
the past century and comparing them to the eustatic rates
provide data to develop predictive model(s) for site-spe-
cific sea level changes over the next century, in the context
of global warming.
Mangrove forests tend to be most diverse and extensive
on tropical sea coasts where there is a net deposition of
sediments and a stable tectonic environment, among other
conditions (Edwards 1995). The mangrove habituated
shorelines have the potential to reveal centuries of histor-
ical sea level variations (Woodroffe et al. 1985). Studies of
coastal peat cores indicate that mangrove systems have the
i
I
i
I
I
I
-I
.- ..1
'~f
_:y
~.
~;
~
. "m·
;;;
~~.
,,'
tf·
i:
ability to keep pace with moderate SLR (Ellison and
¥ Stoddart
J
991; Lynch et al. 1989; McKee et al. 2007;
l
Nyman et al. 2006). Published work has shown that
~' migration and/or mortality of the mangrove halophyte
if
ecosystems can be caused by alterations in the sea level
if
relative to the local sediment accumulation rates (SAR)
N.'
(Blasco et al. 1996; Gilman et al. 2006; Woodroffe et al.
~5
1985). Therefore, acquiring insights into the depositional
f;
and tectonic regimes in conjunction with the local SLR has
j,.
practical use in elucidating the historical condition of a
fc
mangal system and predict its stability.
£.
This papel' examines the stability of a mangrove ecosys-
~, tem located in Cananeia, SE Brazil, in the context of the
f
predicted rise in sea level caused by global warming (IPCC
f
2007). Addressing this, the SAR and temporal variations in
~. the sources of organic matter as well as organic carbon and
:3'~
,c·
organic phosphorus ratios (TOC/OP) were determined. This
f-
r
work demonstrates that the mangrove has remained the
~ predominant source of OM duting the past century [based on
f
stratigraphies of carbon and nitrogen isotopes
(<s
13
C and
'r
(5
15
N) and organic carbon to total nitrogen ratios
(TOCITN)],
'J:
'0
reflecting the stability of the mangal ecosystem. However,
" considering the lower SAR relative to the regional RSL rise
~~. suggests that the
systenl
is prone to being destabilized.
The mangrove habitat under study is located along the
coast of the Cardoso Island State Park
(2S018.40'S
and
48°23.70'W; Fig. 1). This
ISO
km
2
mountainous island, up
to 900 m in altitude, is situated in the Cananeia lagoon-
estuarine system on the southeastern coast of Brazil. The
tidal range within the microtidal environment is ~ 82 em
(Otero et al. 2006). Fresh water influx is by continental
drainage of several small rivers and the Ribeira of Iguape
River, which is the principal source of sediment import to
the estuary (Saito et a1. 2001). The Ribeira Valley is one of
the most actively mined regions for Pb and Zn and for
refining Pb in Brazil. The mining activities began in 1918
and ended in
1995
(Corsi and Landim 2003). The annual
average temperature and precipitation of the region are
~21oC and ~2,200 mm, respectively. Since 1954 this
area has had the longest continuous running tide gauge in
Brazil. Even though this coastal area is generally consid-
ered tectonically stable, an episodic earthquake of 5.2 on
the Richter scale was recorded ~ 200 miles offshore on 22
April 2008.
In 2005 sediment core samples were collected at three sites
along a transect that were located 10 n1 into the mangrove
forest (C3A), mangrove fringe (C3B) and 5 m inside of the
margin in a mud flat (C3C). The cores were obtained by
insel1ing a 7-cm-diameter plastic tube into the substrate
during low tide. The sediment was extruded from the tube
and sectioned at l-cm intervals from the core top to 10 em
and subsequently at 2-cm intervals until the bottom of the
km
r-""9"M ..~. ~_.~
o
5 10
core. A ~ 5-g split of each section was acidified to remove
carbonate, dried and powdered, and a portion was taken for
analyses of organic carbon (OC), total nitrogen (TN), ,,
13
C
and
(5
15
N using an isotope ratio mass sp.~ctrometer (Thermo
Finnigan Model Delta Plus XP), following the method
outlined in Naidu et al. (2000). Organic matter (OM) was
calculated by OC x 1.8 (Trask ]938). From the original
wet section, a split was taken for determining dry bulk
density following Baskaran and Naidu (1995). Granulo-
metric analyses of the sections were done by a CILAS 1064
diffraction laser unit.
Total phosphorus (TP) and inorganic phosphorus (IP)
were extracted from separate 0.4 g of dry pulverized sedi-
ment. The analytical procedures for determination of TP
and IP were according to Grasshoff et a1. (1983) using a
HITACHI model U-I 100 spectrometer. The organic phos-
phorus was derived by subtracting the inorganic phosphorus
from the total phosphorus. The analytical precision was
within 2% for IP and OP. The accuracies of the analyses,
which were tested through certified sediment "NIST"
(Nacional Institute of Standards and Technology, Estuarine
Sediment-1646a), were within 0.0027 ± 0.00 I%, with an
average of 0.0027
±
0.002%, varying by 6%. Pearson
correlation analyses were done with ST ATISTICA software
for Windows, Release 5.1, to verify covariances among TP,
IP and OP.
Sediment accumulation rates for the three cores were
determined by the depth-age relationship of 210Pb and
mCs. For the radionuclide analyses splits of the remaining
core sections were sealed in 70-ml petri dishes for at least
3 weeks to establish secular equilibrium between 226Ra and
214Pb. Gamma-ray measurements were conducted by using
a semi-planar intrinsic germanium high-purity coaxial
detector with 40% efficiency, housed in a lead shield,
coupled to a multichannel analyzer. The 210Pb activity was
determined by the direct measurement of 46.5 keV pho-
topeak, while 226Ra activity was calculated using the proxy
214Pb (351.9 keV) (Appleby et '11. 1988). Activities were
calculated by multiplying the counts per minute for each
radionuclide minus background counts by a factor that
includes the gamma-ray intensity and detector efficiency.
This factor was determined from standard calibrations
using an efficiency curve obtained by measuring and ana-
lyzing a certified standard cocktail of radionuclides; this
standard was certified by IRD (lnstituto de Radioprote«ao e
Dosimetria), certified no. C/87/AOO. The excess 210Pb
(
210
Pb
) .. . d b b . I 2?6R
(ex)
activity was estimate y su tractll1g t le - a
from ·the total 210Pb activity. Samples were counted for
86,000 s in identical geometrical cylinders. Self-absorption
corrections were. calculated following (Cutshall et al.
1982). The sedimentation rate was obtained through the
Constant initial concentration (CrC) approach outlined in
(Appleby and Oldfield 19(2). Sample depth intervals were
normalized for sediment mean fine grain. Cesium-137
activities were determined from the 663.7 keV gamma
peak.
The 21°Pb and 137Cs-based geochronologies of the cores
were supplemented by those based on ages inferred from the
contaminant history of Pb and Zn in the study region. It is
assumed that the first significant increase in Pb and Zn in the
three cores resulted from anthropogenic input consequent to
the initiation of mining of the two metals in 1918. In this
context, the stratigraphic variations in Pb and Zn were
determined in the three cores. To this end, a ~ 2-g split of
each of the core sections was analyzed for Zn and Pb. The
values of the two metals were normalized against Al con-·
centrations in core sections to account for granulometric
differences in the metal chemistry (Mason et a1. 2004). The
AI-normalized Pb and Zn values were then plotted against
the core depths for the three individual cores. "
The three elements (AI, Pb and.Zn) were ·analyzed
through optical emission spectrometry inductively coupled
plasma, using a Job)'- Yvon ULTIMA II spectronieter.
Sediment solutions were obtained by pigestion with a
mixture of nitric acid and hydrochloric acid (4: I), in a
microwave (model MUL TIW AVE of Anton Paar), and the
resulting solutions were filtered with acid-rinsed 0.45 ~lm
membrane. All the material lIsed was pre-cleaned in 10%
HCl and washed with demineralized water. Measurement
errors were within 10%.
Two aspects of the investigation in this work were
addressed: first, on the stability of the mangrove forest
habitat using stratigraphic variations of TOC, TN, TOCI
TN, TP, OP, ()llC(OC) and
c5
15
N. Second, we examined the
SAR in the context of RSL rise in the area and global SLR
models.
The concentrations of TOC, TP and TN in sections of the
three cores are· provided in Table Ia-c. A net significant
decreasing trend may be seen in the depth profiles of the
TOC, TP and TN from the surface, probably reflecting an
increasing degradation with depth in the mangrove litter
(Chen and Twilley 1999; Cahoon and Lynch 1997;
Kristensen et al. 2000; Lallier-Verges et al.
J
998; Lynch
et al. 1989). Further, a relatively greater amount of OM in a
landward direction, coinciding with decreasing tidal influ-
ence, is generally noted. Obviously, this trend is related to
a progressively higher depositional flux of vegetal litter
corresponding to denser and more stable development of
mangrove forest landward (Ferreira et al. 2007).
Environ Earth Sci
Table 1
Organic and metal profile of cores
Depth (em)
TOC(%) TN
(%)
()
13
C
()ION (0/00)
TP
(pg/g)
OP
(flg/g)
Pb/Al"
Zn/Al
a
(a)
..
,
0-2
6.50
0.45
-28.81
1.73
580
350
3.51
20.50
2--4
7.50
0.48
-28.63
0.50
586
269 2.70
9.69.
4-6
6.27
0.39
-28.16
0.06
448
302 2.81
10.85
6-8
6.20
0.37
-28,08
0.20
856
296 3.01
16.87
8-10
5,65
0.30
-28.06
-0.14
356
203
3.51 26.19
10-14
7.07
0.34
-28.17
-0.40
352
235
4.11
37.22
14-18
4.31
0.24
-27.57
1.74
374
198
3.31
19.04
18-22
6.61
0.20
-27.42
1.16
345
203
3.08
20.36
22-26
6.02
0.28
-26.76
0.66
191
150
4.73
41.65
26-30
5,56
0.24
-26.97
1.93
426
107
3.42 21.36
30-34
4.95
0.21
-26.93
2.18
280
80
2,80 18.71
34-38
4.73
0.20
-26.80
2.00
295
96
2.35
16.32
38-42
4.24
0.18
-26.52
2.17
316
116
2.37
11.25
(b)
0-2
6.44
0.48 -27.11
2.87
600
332
1.24
27.05
2-4
7.49
0.50
-27.70
2.71
555
328
1.23
16.61
4-6
7.05
0.47
-27.81
2.71
540
288
1.29
12.53
6-8
7.17
0.45
-27.90
3.22
513
305
1.10
15.49
8-10
5.77
0.35
-27.87
2.92
456
267
1.34
13.19
10-14
5.44
0.29
-27.66
2.99
411
227
1.64
8.31
14-18
3.39
0.17
-27.33
2.88
256
93
2.00
8.71
18·-22
2.96
0.15
-26.96
3.06
296
191
2.88
12.53
22-26
4.00
0.20
-27.30
2.84
291
153
1.47
6.79
26-30
2.80
0.15
-26.78
3.30
319
101
2.38
12.38
30-34
2,92
0.16
-26.90
3.34
287
146
0.98
5.43
34-38
2.62
0.13
-26.62
3.01
292
118
2.91
13.87
38--42
1.81
0.09
-26.82
3.13
314
154
1.65
6.95
(c)
0-2
3.53
0.25
-26.76
2.93
403
221
3.09
10.68
2--4
3.88
0.27
-27.06
2.95
396
236
2.31
8.65
4-6
3.46
0.23
-2701
3.07
313
205
3.05
10.79
6-8
3.65
0.23
-27,24
3.03
292
162
3.12
11.17
8-10
3,60
0,22
-27.41,
3.03
288
151
3.31
12.01
10-14
3.70
0.22
-26.94
3.16
300
194
3.56
12.49
14-18
3.71
0.21
-27,25
3.31
283
122
3.34
11.32
18-22
3,75
0.21
-26.97
3.22
292
164
2.28
9.32
22-26
3.52
0.20
-26,76
3.25
272
129
1.99
8.01
26-30
2.39
0.13
-27,15
2.97
248
94
3.49
12.37
30-34
1.61
0.09
-26.62
3.06
234
114
1.46
5.32
34-38
0.50
0.04
-27.07
3.96
114
16
1.54
4.59
38--42
0.48
0.04
-26.68
3.28
123
I
1.38
3.85
42--44
034
0.03
-26.83
4.33
85
39
1.75
4.01
44--48
0.26
0.03
-26.59
5.02
99
61
1.89
3.22
" AI
x
1,000
It would seem that the TN enrichment in the surface
2(03)
and/or to higher bacterial biomass at the surface. A
layers
is
likely a
result
either
from
tidal
fluxes
ll1
the
scavenging of TN from biological activity or an increasing
inte11idal area by marine particles rich in TN (Allison et al.
mineralization of OM in the subsurface layers of the cores
~ Springer
c-
Environ Eal1h Sci
Table 2
Phy~ical characterization and 210Pbex data of ~ediment core~
Depth (cm)
Dry bulk density
Clay
('Yo)
Silt
('Yo)
Sand
(%)
Poro~ity
('Yo)
210Pbex (Bq/kg)
(a)
\
0-1
0.37
9.8
75.1
15.1
84.89
179.26 ± 18.43
1-2
0.41
9.2
69.8
21.0
83.28
156.19 ± 11.28
2-3
0.38
17.9
65.6
16.5
84.53
153.37 ± 12.32
3-4
0.37
18.1
66.4
15.5
85.13
122.09 ± 9.38 .
4-5
0.42
14.3
64.9
20.8
82.94
124.85 ± 10.10
5-6
0.41
14.0
63.6
22.5
83.11
137.80 ± 12.74
6-7
0.40
16.4
60.9
22.7
83.57
81.47 ± 6.16
7-8
0.46
13.5
50.4
36.1
81.28
85.62 ± 7.16
8-9
0.44
15.4
56.5
28.1
82.19
80.32 ± 6.27
9-10
0.48
14.3
52.3
33.4
80.64
43.29 ± 3.65
10-12
0.45
12.8
45.5
41.7
81.68
35.27 ± 2.65
12-14
0.48
13.9
49.3
36.8
80.51
33.86 ± 2.72
14-16
0.58
15.6
43.8
40.6
76.31
3l.2j7 ± 2.19
16-18
0.58
16.5
46.4
37.1
76.27
27.49 ± 2.08
18-20
0.54
16.9
46.2
36.9
77.97
8.91 ± 0.80
20-22
0.52
18.5
50.6
30.9
78.81
9.75 ± 0.90
22-24
0.52
16.2
43.7
40.1
79.03
12.95 ± 1.30
24-26
0.57
13.9
37.4
48.7
76.79
8.97 ± 0.88
26-28
0.58
12.5
45.7
41.8
76.27
11.88 ± 1.49
28-30
0.64
10.3
38.0
51.7
73.93
11.63 ± 1.29
32-34
0.62
13.7
37.2
49.1
74.74
9.77 ± 1.05
34-36
0.73
14.0
38.2
47.8
70.27
8.41 ± 0.86
36-38
0.84
12.5
41.0
46.5
65.77
-1.84 ± 0.27
38-40
078
11.1
36.2
52.7
68.47
5.78 ± 0.85
40-42
0.64
17.3
40.4
42.3
73.83
-8.53 ± 0.25
42-44
0.64
14.0
32.6
53.5
73.87
0.47 17.1
60.8
22.1
81.09
294.61 ± 22.9
1-2
0.49
17.4
61.6
21.0
80.28
204.19 ± 19.66
2-3
0.43
18.7
67.3
14.0
82.40 322.23 ± 33.10
3-4
0.42
19.1
68.7
12.2
82.95
305.10 ± 32.41
4-5
0.41 17.6
65.7
16.7 . 83.39
311.92 ± 34.67
5-6
0.37
17.2
64.3
18.5
85.06
210.18 ± 19.47
6-7
0.39
17.7
63.5
18.8
84.23
156.90 ± 14.42
7-8
0.46
14.3
51.2
34.5
81.34 260.22 ± 25.28
8-9
0.44
17.5
43.1
39.4
82.34
232.10 ± 24.63
9-10
0.51
20.9
51.5
27.6
79.46 219.23 ± 17.58
10-12
0.58
13.9
46.2
39.9
76.53
129.50 ± 10.02
12-14
0.61
11.2
37.5
51.3
75.19
89.43 ± 7.76
14-16
0.74
13.4
39.7
46.9
70.12
52.08 ± 4.06
16-18
0.75
9.0
26.8
64.2
69.78
68.90 ± 5.91
18-20
0.75
12.2
32.6
55.2
69.33
42.24 ± 3.88
20-22
0.79
10.4
27.8
61.8
68.14
36.06 ± 3.65
22-24
0.77
14.3
45.3
40.4
68.48 58.75 ± 6.68
24-26
0.78
8.4
26.7
64.9
68.11
17.33 ± 1.79
26-28
0.77
8.3
32.3
59.4
68.51
23.80 ± 2.24
28-30
0.76
7.3
28.5
642
69.16
23.15
±
2.16
Environ Earth Sci
Table 2 continued
Depth (cm)
Dry bulk density
Clay
('Yo)
Silt
('Yo)
Sand
('Yo)
Porosity
(%)
21llPb
ex
(Bqlkg)
32-34
0.73
\ I 1.0
36.2
52.8
70.38 4.54 ± 0.38
34-36
0.83
9.8
32.4
57.8
66.49
\3.64 ± 1.09
36-38
0.85
6.6
24.1
69.3
65.55
7.15 ± 0.70
38-40
0,70
11.7 42.9
45.4
71.49
20.98 ± 2.37
40-42
0.89
9.2
36.7
54.\
63.98
-8.53
±
0.97
42-44
0.99
9.8
39.1
51.\
59.96
(c)
0-1
0.68
7.5
66.0
26.5
72.67
104.52 ± 4.47
1-2
0.66
7.0
62.0
3\ ,0
73.08
93.49 ± 5.71
2-3
0.66
8.8
62.3
28.9
73.39
94.\3 ± 6,23
3-4
0.63
9.0
63.6
27.4
74.49
94.54
±
4.73
4-5
0.61
12.5
59.1
28.4 75.12
94.74 ± 4.73
5-6
0.69
13.0
61.8 25.2
71.85
\00.53 ± 4.91
6-7
0.64
7.9
63.5
28.6
74.09
\04.50 ± 4.66
7-8
0.61
7.4
60.1
32.5
75.73
98.54
±
4.71
8-9
0.65
11.4
52.2
36.4 73.57
100.44
±
4.82
9-10
0.68
12.1
55.4
32.5
72.58
85.48
±
3.69
10-12
0.65
12.1
51.4
36.5
73.53
60.2\
±
2.32
12-14
0.71
10.4
44.4
45.2
71.32
59.15
±
2.32
14-16
0.70
9.1
45.6
45.3
71.72
29.45
±
1.24
16-18
0.69
10.1
50.6
39.3
72.16
50.1\
±
2.22
18-20
0.71
13.2
55.7
31.\
71.27
37.35
±
1.73
20-22
0.61
12.7
53.4
33.9
75.24
28.0\
±
1.62
22-24
0.74
10.4
43.6
46.0
69.99
23.35
±
1.29
24-26
0.82
10.0
42.0
48.0
66.94
25.10
±
1.27
26-28
0.88
10.3
45.8
43.9
64.45
15.75
±
.092
28-30
0.94
10.1
44.8
45.1
61.96
10.\5
±
0.60
32-34
0,91
9.2
45.8
45.0
63.30
\0.85
±
0.64
34-36
1.07
9.3
46.5
44.2
56.62
11.51
±
0.70
36-38
1,13
8,8
42.0
49.2
54.39
-0.32
±
0.02
38-40
1.16
12.1
57.3
30.6
53.10
2.79
±
0.1\
40-42
1.19
12.7
57.3
300
51.81
-0.89
±
0.05
42-44
1.22
11.9
53.3
34.8
50.40
2.54
±
0.19
44-46
1.27
12.4
52.7
35.0
48.48
4.13
±
0.30
46-48
1.33
12.4 52.7
35.0
46.20
-0.54
±
0.04
48-50
1.26
11.4 45.4
43.2
49.09
0.39
±
0.69
may explain a slight decrease in the TN concentrations
down core. Other studies suggest that this profile is char-
acteristic of a recent introduction of fresh OM from vas-
cular plants to surface sediments (Lallier-Verges et al.
1998; Marchand et al.
2(06).
Phosphorous concentrations may also provide insight
into OM origins in marine sediments (Mach et al.
1(87),
specifically based on OC/OP ratios (Ruttenberg and Goni
19(7). For instance, terrestrial plants have values
between 300 and 1,300 (Ruttenberg and Goni 1(97),
,while marine phytoplankton has an average of approxi-
mately 100 (Redfield et al.
1(63).
Consideration of the
sediment OC/OP values (average value of 253 and
ranging from 43 to 621) indicates marine input and/or a
rapid immobilization of OP that may occur during OM
decomposition (Tables I, 2) (Alongi 1991; Holmboe
et al. 200J).
The overall close ranges of TOC/TN and TOC/OP of the
cores (Table I) suggest a consistent depositional flux of OM
perhaps derived from the same source. As mangrove eco-
systems have a high capacity of retaining and recycling most
nutrients within the sediment column (Kristensen et al. 2000;
Twilley et al.
1(86),
this trend may be expected in a robust
mangrove forest.
,'j
"'I::
i'i
" ,'JI
~~;:~:;H~:g::~~;~~;~;Vi;~\£~{i;;iFi~~~:~f~.:;'::":"'"',(,
i,:,',i~!
of the above IS that the mangal forest in the study area has ,
1
remained stable during the past century and that the',<,
,Ii
stratigraphic variations are of a typical mangrove forest", ' ';
ii
<11
r'
if
~;
"H
ii
. Ii
,I;
~I
Ii
II
li
~
:
iJ
.'
':!
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I
!
i
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, !
Although increased down-core degradation of OM may
occur, the signature of the sources of sediment OM most
likely remains preserved in sediment cores as expressed in
their carbon and nitrogen isotopic:c'omposition (Meyers
1994). This is likely the case in this study area, as indicated
by the bl.1C
tOCJ
and b
15
N results (Table la-c),
As mangrove vegetation is unique in that it survives in
specific intertidal zones, specific geochemical proxies have
been implied for the three core locations to better under-
stand the characterization of the sediment being depositing
in each specific region of the mangrove system. Core C3A
displays general enrichment in the ()13C(OC) in the lower
depths of the profile. This trend may be explained by rel-
atively longer microbial respiration down the core that
induces an isotope fractionation depleting mineralized CO
2
in 13C and enriching residual degraded particulate OM in
13C (Mariotti and Balesdent 1990; Mazuka and Shunula
2006). As core C3A is within the higher reaches of the
forest and is inundated by tides for relatively shorter
periods of time, this site is aerated for longer time intervals,
thus increasing the oxidation of the OM being deposited at
this site, Cores C3B and C3C are situated in the margin and
mud flat region of the mangrove ecosystem, being inun-
dated for longer periods of time, Because isotopic changes
due to OM degradation are less significant in areas under
the water surface, there is an expected smaller variation in
the
b
13
C(oc)
along these cores (Lallier-Verges et al. 1998;
Lehmann et al. 20(2),
In mangrove systems, sediments further inland typically
have lower
b
15N values (Fry et al. 2000), as is the case for
core C3A, These lower ()
15
N values may be associated to
the higher concentrations in OM, favoring a fractionization
by plants that selectively choose 14N, thereby increasing
the 15N concentrations, reflected in sediments having lower
b
l5
N values (Mazuka and Shunula 2006), Another possible
factor in the higher ()15N in core C3B and C3C is that they
are in areas of the tidal flat being exposed to tidal inun-
dation for longer periods of time. As oceanic" nitrate has
relatively higher ()
15
N, tidal inundation plays a larger role
in the C3B and C3C than in the C3A b
l5
N values, which is
less significant farther inland (Table Ia-c).
The relatively low ()!3C(OC) and (j15N are typical values
relating to a terrestrial OM source, likely from mangrove
vegetation (Naidu et al. 2000 and references therein;
Bouillon et al. 2003, 2004; Lallier-Verges et al.
J
998;
Mazuka and Shunula 20(J6; Woller et a!. 2(03). The con-
sistent similar values throughout the cores in the carbon
and nitrogen isotopes (()
13
C and b
15
N) and TOC/N suggest
that the sources of OM for the mangal forest has been
invariable during the past ~ 100 years and that the source
has been terrigenous and likely local from the mangallitter.
Indeed, when the values of ()
I
3C(OC) are plotted against
those of TOC/TN, the scatter plots lie in a cluster that is
A net down core decrease in 210Pbtcx) activities is seen in
all three cores (Table 2a-c), which can be attributed to a
few factors. The varying mud content «63 J.un size frac-
tion) in the cores (Table 2a-c) could be a factor in the
2IoPb(cx) distribution (Ravichandran et al. 1995). However,
in this study the granuJometric influence was In,~nimized by
normalizing the 2IoPb(cx) activities to the mud fraction
(Table 2a-c). After normalization, the log profiles of
2IoPb(cx) were found to decrease linearly down the care
(Fig. 3a-c), implying a consistent rate o,fsedimentation
(Appleby and Oldfield 1992). Following this, the CIC
dating method was applied to establish the geochronology
of the three cores. The statistics related to the cores'
210Pb(cx) distribution are in figures and as follows: C3A
(n
=
15;
P
<
0.05) from the surface to the 19 cm mark;
C3B
(n
= 16; p
<
0.05) 6.5 to the 35 cm interval; C3C
(n
=
14; p
<
0.05) between the 6.5 and 33 cm depth.
Apparently the upper 6,5-cl11 layers in cores C3B and
C3C were reworked and, therefore, excluded in the above
statistical analyses. In the mangrove forest core (C3A), the
absence of a mixed surface layer agrees with the fact that
0
0
-5
-10
-15
0
0
-20
-,
"0
-25 '
-30
Toe/TN
20
---<>--C3A
..••..-C3B
•• C3C
y=
-O.12x
+
557
R' =0.90
eo
5
~ 4.5
X
:3
4
N
~ 3.5
.5
10
Depth (em)
y =-O.llx + 6.68
R'
=
0.85
6.0
cD 5.5
~
g
5.0
;,-
.-
=:
N
..b
Q., 3.5
3
.10
0
(c)
~.~
~
OD
~
""
4.5
:<l
.~
4.0
'"
=:
N
3.5
..b
c..
3.0
Z
..:l
25
2.0
0
15 20 25
Depth (<:m)
y
=
-0.09x
+
5.5 I
R' =0.92
I"" I"" I"" I"" I' ,., I"" I
5 10 15 20 25 )0 35
Depth
(tm)
Fig. 3 Mud-normalized 21°Pb<x distribution as used for SAR;
a C3A
=
2.5
mm year-
J
,
b C3B
=
2,9
mm year-I, c C3B
=
3.9 ml11year-
t
bioturbation and physical reworking of sediments may be
negligible within salt marshes (Zwo!sman et al.
J
(93),
Along the transect, the SAR increased from 2.5 and 2.9 to
3.9 mm year-I, respectively. The
1.1
7
Cs activities, which
are often used to confirm the crc 210Pb dating model
(Sanders et al. 2006), were above the detection limits in all
except a few sections from specific depths of the cores, The
depth where 137Cs activity is highest was considered to
correspond to 1963, based on which there was a SAR of
2,6 mm year-I in the central forest (C3A), 3.4 mm year-I
in the forest margin (C3B) and 3.9 mm year-I in the mud
flat (C3C). Therefore, in this study the SAR estimates
based on 1J7Cs markers are in close agreement with those
based on the 210Pb model (Fig, 4).
Environ Earth Sci
0 0.5
0
5
S
10
~
..<::
15
C.
•..
Q
20·
25
1.17
Cs (Bq/I<g)
1.5 2 2,5
o C3A
• C3B
••. C3C
1963
-/
(~::::)
.• -
Sediment accumulation rates were also estimated through
evidence left by trace metal (Pb and Zn)' contamination
from mining activity adjacent to the study area. The AI-
normalized Pb and Zn contents in the cores are listed in
Table Ia-c. A sharp increase in the Pb/AI and Zn/Al ratios
can be seen in the C3A core at the 24-cm mark. The C3C
core shows a relatively less dramatic spike in both Pb/AI
and Zn/ Al ratios at the 28-cm mark. However, no clear
relative Pb/AI or Zn/AI sedimentary shifts were identified
in the C3B core. The spikes identified in cores C3A and
C3C are assumed to coincide with Zn and Pb mining
activity in 1918 (Corsi and Landim 20(3). Considering the
year (1918) mining activity and assuming steady sediment
depositional flux since then, SAR were obtained as follows:
2,7 mm year-I in the central mangrove forest (core C3A)
and 2.5 mm year-I in the mud flat (core C3C). These rates
are comparable to those based on the 210Pb and 137Cs
methods.
The Cananeia SARs are significantly lower than the local
net sea level rise (SLR) as recorded by the nearby time-
series tide gauge. This tide guage indicated that the sea
level rose approximately 4.0 mm year-I from 1954 to
2004 (Fig, 5, after the University of Hawaii http://www.
soest.hawaii,edu/UHSLC/, run through the NIMED
program). TI1e SARs estimated for this study area (2,5-
3,9 111myear-I), used to imply RSL, are substantially
higher than the rates found in mangrove forests further
nonh (Sanders et al. 2008; Smoak and Patchineelam 1999),
~ J.8 mm year-I. Explanations for the discrepancies
between the SAR and SLR mentioned above are:
Fig. 5 Yearly tide gauge
records from 1954 to 2004
"
.
,
,
, ,., #
o·
-t-··I·-j····t-·I·-f···t·-!···H··++-l-+-+++··t-+·i·-i-+··t····1·'·I·!.·j:·'+-';-f-~-t-~j..!.;-t-H+I
, , .I" "
,
I.
Relative sea levels (RSL) may vary from one region to
another (Harvey et a!. 2002); therefore, rates indicative
of a sea level rise (SLR) taken further north may not be
comparable to this area. This is particularly true in
Cananeia, which on 22 April 2008 was found by the
USGS to be tectonically unstable, as has been noted by
the recent offshore earthquake of 5.2 on the Richter
scale.
2. As the Cananeia tide gauging only began
SO
years ago
and large decadal variation is seen in this record
(Fig. 5), the duration may not be sufficient to detect an
accurate sea level trend. This point is well made by
Pirazzoli (1986) and is evident in this study area.
3. Given these parameters, assertions based on factors
other than the eustatic sea level rise are affecting this
region, and the global models may not apply for
determining current and future rates in this aJ~ea.
From the onset of this study, it was thought that the study
area was tectonically s~able, but could not explain the tide
gauge data nor, after results were obtained, the relatively
high sedimentation rates in this stable mangrove forest.
That was until an earthquake was measured offshore in
April 2008. The tectonic instability in the region may
explain the relatively high RSL rise inferred by the tide
gauge (50 years) as well as the stable SARs (over
100 years) found in the mangrove forest. As these data
were not in agreement with estimates of the global mean
SLR of 1.7 ± 0.3 mm year-I [from 1870 to 1992 (WCRP
2006»), it is suggested that factors other than the eustatic
sea level rise are affecting the sea level changes in this
Brazilian region. This being so, global models to predict
future rates of SLR as presented by the IPCC (2007) must
be considered with some caution.
This study in the Cananeia mangrove system demon-
strates that the RSL could vary from one coastal area to
another. Therefore, to predict the affect of eustatic sea level
rise on any gi ven coastal region, it is critical that local, site-
specific estimates of SLR must be elucidated. We also
show the importance of determining the SAR on global
SLR models, especially where tide gauges have not yet
been installed or not been in use for a period of time suf-
ficient to deteI'm
j
ne sea level trends.
Acknowledgments This work was funded by the Conselho Nac-
ional de Oesenvolvimento Cientrfico e TecnoJogico (CNPq). Brazil.
and Fulbright support to 1.M.S. We would like to acknowledge the
Instituto de Radioprotecao e Oosimetria (IRO) for supplying a
cenified radionuclide cocktail that was used for calibrating the
gamma-ray detector. The cost of the analyses of the sediment
carbon and nitrogen and their isotopes were met from funds
available to A.S.N. from the Instilllte of Marine Science. University
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.
~~~,
.
-
~~
{
.
5.3 TENDENCIAS NA SEDIMENTA<;AO NAS MARGENS DE MANGUEZAIS,
INFERlNDO UM MIGRA<;AO CONTINENTAL DA FLORESTA
--\
Dois testemunhos de sedimentos- foram coletado nos margens de manguezals bem
desenvolvido para estudar a relac;ao entre
0
aumento no nivel do mar e a taxa de sedimentac;ao. 0
SANDERS, C.J.; SMOAK, J.M.; NAIDU, A.S.; BRANDINI, N; SANDERS, L. M;
PATCHINEELAM, S.R. Sedimentation patterns in mangrove margins, inferring continental
forest migration,
Sedimentary Geology,
in review .
Elsevier Editorial System(tm) for Estuarine, Coastal and Shelf Science
Manuscript Oraft,
Title: Organic carbon burial from mangrove to intertidal mud flat; sedimentation and sea level rise
Keywords: Pb-Z10, oCl3, oN15, Tamandare, Brazil
Corresponding Author's Institution: Universidade Federal de Fluminense
Order of Authors: Christian Sanders, PhO; Joseph M Smoak, PhO; Sathy Naidu, PhO; Luciana Sanders;
Sambasiva R Patchineelam, PhO
Abstract: This work quantifies the organic carbon (OC) flux from mangrove to mudflat sediments in the
northeastern region of Brazil (Tamandare, Pernambuco). Sediment characterization (OC13, oN51,
OC/TN and mud fraction) indicated a representative mangrove system. Sediment cores were taken in a
transect (forest, margin and mud flat) to calculate sediment accumulation rates (SAR) of 2.8,5.0 and
7.3 mm/year, giving OC burial rates 353,949,1129 (g/m2/year), respectively. The results of this study
indicate an increasing trend of SAR's and OC flux from within the mangrove forest to the intertidal mud
flat.
Suggested Reviewers: Thomas
J
Smith PhO
USGS
tom_Lsm [email protected]
v
Wanilson L Silva PhO
Professor, Geology, UNICAMP
wa [email protected]
~~
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Organic carbon burial from mangrove to intertidal mud flat;
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Christian J. Sanders
l
',
Joseph M. Smoak
2
,
A. Sathy Naidu
3
,
Luciana M. Sanders
4
,
Sambasiva R. Patchineelam
l
I
Universidade Federal de Fluminense (UFF), Departamento de Geoqufmica, Niler6i-RJ, Bra:::il
2 University of South Florida (USF), Environmen/al Science, St. Petersbwg, FL, U.SA.
3
University of Alaska Fairbanks (UAF), Institute of AilarineSciences, Fairbanks, AK, U.SA.
~Istiluto de Radioprotecao e Dosimetria (IRD), Rio de Janeiro 22780. Bra:::il.
*Corresponding author. E-mail addresszinosanders@yahoo.com
Morro de Valonguinho 24020 - 007 Niteroi, RJ, Brazil
Telephone; (2
J)
8332-0948/ (21) 2629-2200
proxies include carbon, nitrogen isotopes
(c
13
e
and C
I5
N) (Lallier-Verges
et al.,
1998;
~.,
~:
~,
r:
~'
t~
W
!
IQ:'
IV
Iii
IJ'
11
19'
f9
(1
f8:
19·
io"
it:
It
13
1~
15.
16;
1;7.
18
19
1,0;
Jl
j~:
1j'
J4
35
J,o,
n
18
J9
(0
IF
~2
o
t4
~5':
f6
n
~8
~9
50
51
52
1~3
1),4,:'
1
55
~56
I,
)7'
58
, 59
," 60
': 61
,:' 62:
;. 63
t~;
daughters 214Pb and 214Bi
(295.2
KeY)
(351.9
KeY)
(609.3
KeY) (Moore,
1984).
The
excess 210
Pb
C2lOPbcex))activity was estimated by subtracting the 226
Ra
from the total 210
Pb
.,
introduction of fresh OM from vascular plants to surface sediments ( Lallier-Verges °et
size fraction) in our cores (Table 2a, b and c) could be a factor in the
2lO
Pb
(ex)
distribution
minimized by normal izing the 210Pb(ex)acti vities to the mud fraction After normalization,
'.
the log profi les of 21°Pb(ex)were found to decrease almost Iinearly down the cores (Figure
2a, b and c), implying a consistent rate of sedimentation (Appleby and Oldfield, 1992).
Following these data sets, the CIC dating method was applied to establish, the
geochronology of the three cores. The statistics related to the cores' 2lOPb(ex)distribution
are as follows; T5A (n=16; p< 0.05) Y = -0.043x + 4.264 R
2
= 0.935; T5B (n=21; p<
0.05) y = -0.062x + 4.339 R
2
= 0.839; T5C (n=12; p< 0.05) Y= -0.1 09x + 4.602 R
2
=
0.941. Along the transect, the sediment accumulation rates (SAR) increased from 2.8,
Since mangrove ecosystems are considered areas where large quantities of OC are
sequestered and a source to oceans, OC fluxes were calcu lated for each area. Due to the
relatively high sediment accumulation rates and OM content in the mangrove mudflat and
margin, significantly higher OC burial rates were calculated than the flux within the
forest (Figure 5). Similar findings were reported for mangrove fringes in (Chmura et aI.,
2003). The data in figure 5 are particularly striking when compared to global averages
are less 300 g/m
2
/year. The results of this study suggest that mangrove intertidal mudflats
be
considered significant when compiling budgets associated with the mangrove OC
budgets. Furthermore, coastal mudflats may be more susceptible to an increasing sea
accompany sea level oscillations (Alongi, 2008; Lynch et aI., 1989; Sanders et al., 2008).
From the global OC budget estimates in (Bou ilion et aI., 2008b) it was illade clear
that a substantial gap in the OC budget was unaccounted for in the global estimates.
From the present study, it is apparent that large fluxes of OC originating from mangrove
forests (as indicated by OM proxies) are being buried in the mudflats associated to these
forests. Given the assumptions made in this paper, there is of lack of information leading
to the processes were by the OC is transported to these areas. Understudying the role of
the mangrove systems in terms of the global OC sequestrations is significant considering
a rising sea level and encroaching agricultural in areas such as Brazil. Sea level rise and
OC budgets are of concern due to the lack of knowledge when compiling global carbon
This work was funded by the Conselho Nacional de Desenvolvimento Cientifico e
Tecnol6gico (CNPq), Brazil and Fulbright support to J.M.S.
Allison, M., A., Khan, S., R., Goodbred Jr, S., L. and Kuehl, S., A., 2003. Stratigraphic
evolution of the h~:teHolocene Ganges - Brahmaputra lower delta plain.
Sedimentary Geology 155,317-342.
Alongi, D.M., 2008. Mangrove forests: Resilience, protection from tsunamis, and
responses to global climate change. Estuarine, Coastal and Shelf Science 76, 1-13.
Bouillon, S. et al., 2008a. Mangrove production and carbon sinks: A revision of global
budget estimates. GLOBAL BIOGEOCHEMICAL CYCLES 22,1-22. ,
Bouillon, S., Connolly, R.M. and Lee, S.Y., 2008b. Organic matter exchange and cycling
in mangrove ecosystems: Recent insights from stable isotope studies. Journal of
Sea Research 59,44-58.
Cahoon, D.R. and Lynch, c., J., 1997. Vertical accretion and shallow subsidence in a
mangrove forest of Southwerstern Florida, U.S.A. Mangroves and Salt Marshes 1,
173-186.
Chmura, G.L., Anisfeld, S.c., Cahoon, D.R. and Lynch, J.c., 2003. Globed carbon
sequestration in tidal, saline wetland soils. GLOBAL BIOGEOCHEMICAL
CYCLES 17, 1-12.
Horton, B.P., Zong, Y., Hillier, C. and Engelhart, S., 2007. Diatoms from Indonesian
mangroves and their suitabitlity as sea-level indicators for tropical environments.
Marine Micropaleontology 63, ]55-168.
Lallier-Verges, E., Perrussel,B.P., Disnar, J. and Baltzer, F., 1998. Relationships
between environmental conditions and the diagenetic evolution of organic matter
derived from higher plants in a modern mangrove swamp system (Guadeloupe,
French West Indies). Organic Geochemistry 29, 1663-1686.
Lynch, c., 1., Meriwether, J.R., McKee, B.A., Vera-Herrera, F. and Twilley, R.R., 1989.
Recent Accretion in Mangrove Ecosystems Based on Cs-13 7and Pb-21 O.
Estuaries 12,284-299.
Marchand, C. et aI., 2006. Heavy metals distribution in mangrove sediments along the
mobile coastline of French Guiana. Marine Chemistry 98: 1-17.
Moore, W.S., 1984. Radium Isotope Measurements using Germanium detectors. Nuclear
Instraments and Methods 223, 407-411.
Sanders, c.J., Santos, I., R., Silva, E., V. and Patchineelam, S.M., 2006. Mercury flux to
estuarine sediments, derived from Pb-21 Oand Cs-13 7 geochronologies
(Guaratuba Bay, Brazil). Marine Pollution Bulletin 52, 1085- 1089.
Sanders, C.J., Smoak, J.M., Naidu, A.S. and Patchineelam, S.R., 2008. Recent Sediment
Accumulation in a Mangrove Forest and Its Relevance to Local Sea Level Rise
(llha Grande, Brazil). Journal of Coastal Research 24, 533-536.
Sanders, C.J. et ai., 2009. Mangrove forest sedimentation and its reference to sea level
rise, Cananeia, Brazil. Environmental Earth Sciences. in press.
Twilley, R.R., Lugo, A., E. and Patterson-Zucca,
C.,
1986. Litter production and turnover
in basin mangrove forests in southwest Florida Ecology. 67, 670-683.
Figure
1.
Study Area
t
Figure 2. Mud-normalized 210Pbexdistribution as used for SAR.
Figure 3. OC/ TN vs depth.
Figure 4. TOC vs 8
13
C(OC).
Figure 5. Organic carbon flux in the mangrove forest (T5A) Margin (T5B)
Inteliidal mud flat (T5C).
High tide
-----_...:.--------
Low tide
\ 10
(111)
TAA
\ 20
(111)
TAB
\
,
TAC
y
=
-0043x
+
4.264
R
2
=
0.935
0)
..>::
S-
35
X
~ 3.3
..-
~
.n
e:.
3.1
z
-l
2.5
o
20 25
Depth (em)
4.5
4
OJ)
~
.....•.
0-
3.5
~
,.-...
x
OJ
0
3
,....;
N
I
..a
0...
'--'
2.5
Z
...:l
2
1.5
0
y = -0.062x + 4.339
R
2
=
0.839
.
I
,
,
I
,
I
I
,
I
I
I
I
I
I
I
I
5
10
15
20
25
30
35
Depth (em)
!
(b)
,!),
4
.•.
.•.
3.5
.•.
C!J
.•.
..:::::
.•.
-...
.•.
0-
00
,......,
3
x
Q)
0
...-<
N
I
.0
2.5
Cl-<
'-'
Z
...:l
2
y
= -0.1 09x + 4.602
R
2
=
0.941
Figure 3.
t
OC/TN
15
18
21
24
27
30
33
0
5
10
E
~
15
-=
.•...
0-
20
OJ
Cl
25
30
-o-T5A
<:s
35
T58
40
-.-T5C
45
15
-25
-26
-26
U
-27
;::
r.Q
-27
-28
-28
OT5A
T5B
.•.T5C
TSA
Depth (em)
0-1
1 - 2
2-3
3-4
4-5
5 - 6
6 - 7
7-8
8 - 9
9 - 10
10- 12
12 - 14
14 - 16
16 - 18
18 - 20
20 - 22
22 - 24
24 - 26
26 - 28
28 - 30
30 - 32
32 - 34
34 - 36
36 - 38
38 - 40
0.36
0.39
0.37
0.35
0.40
0.40
0.39
0.43
0.41
0.45
0.42
0.45
0.54
0.54
0.50
0.49
0.48
0.52
0.53
0.57
0.56
0.65
0.73
0.68
0.59
-26.32
-26.39
-26.18
-26.25
-26.50
-26.29
-26.45
-26.34
-26.08
-26.42
-26.18
-26.39
-26.37
-26.24
-26.39
-26.45
-26.51
-26.43
-26.09
-25.83
-25.99
-25.88
-25.92
-25.86
-25.85
1.54
1.42
1.84
1.68
1.48
0.81
1.62
1.29
1.19
1.29
1.41
2.17
1.68
1.86
1.35
1.27
1.25
1.36
1.48
1.46
1.25
0.90
1.30
1.77
1.32
TN(%)
OC (%)
Mud
(%)
0.47
9.30
76.52
0.51
10.70
74.84
0.46
8.63
70.23
0.44
8.48
66.80
0.43 8.49
77.07
0.50
11.07
73.53
0.53
10.68
79.69
0.53
11.18
79.13
0.43
9.17
74.77
,.j
0.42
8.86 64.95
0.36 7.59 67.84
0.36 7.83
63.45
0.40
8.61 66.96
0.44
9.83 62.36
0.45
10.85
62.48
0.44
9.86 64.58
0.37
9.38 70.55
0.31 7.58
69.39
0.43
10.96 70.72
0.49
13.54
76.13
0.43
11.60 73.13
0.32 8.94 76.54
0.43
11.88
72.48
0.37
9.91 70.66
0.42
12.04
71.38
~.' Organic and physical data takenfrom the T5A sediment core profile, Dbd indicates dry bulk
I~
dens;/y.
~t
.~~
'F
Table 1 (b).
t
T5B
Depth
(em)
Dbd (g/cm
3
)
Jl3
e
J1sN
TN(%)
oe
(%)
Mud (%)
0-1
0.47
-26.21
1.68
0.66 12.32
81.75
I - 2
0.49
-26.04
1.93
0.64 11.71 55.74
2-3
0.43
-26.03
2.55
0.62
11.46
84.98
3 - 4
0.42
-26.06
1.74
0.63 12.30
95.00
4 - 5
0.41
-26.24
1.98
0.58
11.44
94.90
5-6 0.37
-26.38
1.83
0.58 12.28 70.52
6-7 0.39
-25.99
1.77
0.59 11.72 80.04
7 - 8
0.46
-26.08
1.62
0.62 12.75 76.66
8 - 9
0.44
-26.16
1.55
0.54 10.99 68.87
"
9 - 10 0.51
-26.07 2.01
0.62
11.24 59.16
10- 12 0.58 -26.36
1.72
0.52 10.61
53.34
J2 - 14 0.61
-26.59 0.98
0.41
11.34
53.45
14 - 16
0.74 -26.26
1.40
0.56
16.47
55.13
16 - 18 0.75
-26.32 0.50
0.44
11.97
49.72
18 - 20
0.75
-26.47
1.56
0.29 7.57 47.83
20 - 22 0.79
~26.09
0.25 0.29 8.55 52.56
22 - 24 0.77
-26.00
1.01
0.42
11.29
59.24
24 - 26
0.78 -25.77
1.06
0.38 9.54 73.77
26 - 28 0.77 -25.81
1.87 0.48
11.92 66.35
28 - 30 0.76
-25.78
1.90 0.46
10.47 81.41
30 - 32
0.73 -25.54
1.42
0.49
11.88
82.00
32 - 34 0.83 -25.52
1.85 0.46
11.34 70.89
Organic and physical daza taken from the T5A sediment coreprofile, Dbd indicates dry bulk
density.
Table 1 (c).
~
T5C
Depth
(em)
Dbd (g/cm
3
)
b
13
C b
15
N
TN
(%)
OC
(%)
Mud
(%)
0-1
0.68
-26.10
l. 11
0.33
6.39
60.90
] - 2
0.66
-26.25 0.71 0.25
5.53 64.57
2 - 3
0.66
-26.] 1
0.74
0.47
8.72
65.00
3-4 0.63
-26.23
1.16
0.30 5.71 65.82
4-5 0.61
-26.40
0.87
0.54
11.13
74.07
5 - 6
0.69
-26.30
0.39
0.50
10.55
73.09
6-7
0.64 -26.22
1.06
0.39
8.]4
61.25
'"
7 - 8
0.61 -26.25 0.79
1.05
21.42
63.91
8 - 9
0.65
-26.36 0.34
0.37
8.49
66.88
9 - 10 0.68
-26.04
1.25
0.63 12.10
60.92
10 - 12
0.65
-26.22
1.03
0.39 8.16 62.25
12 - 14
0.71 -26.08
0.49
0.33
7.06
62.50
14 - 16 0.70
-25.89 0.75
0.46
10.60
55.71
16 - 18
0.69
-25.72
0.93
0.51
11.68 50.74
18 - 20
0.71
-26.16
0.46
0.17 5.64
45.71
20 - 22 0.61
-25.77
1.02 0.33
8.38
26.60
22 - 24 0.74
-25.85 0.55
0.14 3.91
23.15
24 - 26
0.82
-25.65 -0.65 0.04
1.09
28.37
26 - 28 0.88
-25.86 -0.28
0.12 3.79
12.11
28 - 30 0.94
-25.85
1.08
0.15 4.51
14.06
30 - 32
0.91 -25.93
1.55
0.] 7
4.51 23.86
32 - 34
1.07.
-25.84
0.43
0.28
8.16
30.85
34 - 36
1.13
-25.94
0.07
0.11 3.09
16.34
36-38
1.16
-25.70
1.15
0.14
3.40
23.01
38 - 40
1.19
-25.86
1.29
0.15
3.72 22.96
40 - 42
1.22
-25.93
1.45
0.22 5.85
33.01
42 - 44
1.27
-25.93
0.48
0.10 2.57
19.20
44 - 46
1.33
-25.89
1.06
0.13 3.38
26.55
Organic and physical data taken from the T5A sediment core profile, Dbd indicates dry bulk
density.
Elsevier Editorial System(tm) for Sedimentary Geology
Manuscript Or't,ft
Keywords: sediments accumulation rates, sea level rise, sand, Pb-2l0, OM, chlorophyll-a/pheo-
pigments
Order of Authors: Christian Sanders, PhD; Joseph Smoak, PhO; Nilva Brandini, PhO; Luciana Sanders;
Sambasiva Patchineelam, PhO
Abstract: Two sediment cores were collected at the margins of well developed mangrove forests to
study the relation between the relative sea level rise and sediment accumulation rates (SAR). A 2l0Pb
dating model (CIC) was used to determine SAR's. Initial results indicate stable SAR's of - 2.0 mm/year
at both sites. Since the two sediment cores in this study were taken on the mangrove margins, if forest
migration existed, this area would be sensitive to changes in sediment regimes, including vegetal
deposition. The similarity in the profiles of these two cores, -50 km apart, indicate a recent change in
the depositional patterns. Recent sand, chlorophyll-a and pheo-pigment enrichment and decreasing
OM (dry wt
%)
during the time period considered (-100 years or 20 em depth) indicate landward set
back of coastal forests in this region.
ript
re to download Manuscript: SG_.Sanders_et_aI.2009_PA_GA_paper - Copy.doc
Sedimentation patterns in mangrove margins, inferring continental forest migration
\!>
Christian J. Sanders
1
*, Joseph M. Smoak
2
, Nilva Brandini.
1
, Luciana M. Sanders
3
,
Sambasiva R. Patchineelam \
I
Universidade Federal de Fluminense (UFF) , Deparlal71ento de Ceoq/lil71ica. Niter6i-RJ 24020, Bra::il
lUniversity of South Florida (USF) , Environl71enlal Science, St. Pelershlllg, FL, 33701 US.A.
31stituto de Radioprolecao e Dosil71etria (IRD). Rio de Janeiro 22780, Bra::il.
Abstract
Two sediment cores were collected at the margins of well developed mangrove forests tp
study the relation between the relative sea level rise and sediment accumulation rates
(SAR). A 210Pbdating model (CIC) was used to determine SAR's. Initial results indicate
stable SAR's of ~ 2.0 mm/year at both sites. Since the two sediment cores in this study
were taken on the mangrove margins, if forest migration existed, this area would be
sensitive to changes in sediment regimes, including vegetal deposition. The similarity in
the profiles of these two cores,
~SO
km apart, indicate a recent change in the depositional
patterns. Recent sand, chlorophyll-a and pheo-pigment enrichment and decreasing OM
(e1ry wt %) during the time period considered (~I 00 years or 20 cm depth) indicate
landward set back of coastal forests in this region.
Key words; sediments accumulation rates, sea level rise, sand,
210
Pb, OM, chlorophyll-a.
pheo-pigments
*Correspond ing author. E-mail [email protected]
water movement to speeds conductive for particle settlement (Cahoon and Lynch 1997;
Young and Harveya 1996). Mangrove ecosystems are also know to be efficient carb;n
associated to sea level changes during the past 1000 (Cohen et al. 2005). Vegetation
."
shifts within the previous ~ 5000 years have been linked to sea level oscillation in
(Figure I). They are surrounded by well-developed mangrove forests and furnished with
B
measmement of
46,5
KeY gamma peak, while
226
Ra activity was calculated using
214Pb
Radioproteyao e Dosimetria), certified nO
C/87/AOO,
The excess
210Pb C2IOPb(ex»)
activity
226 ?\O
was estimated by subtracting the Ra from the total - Pb activity. Samples were
counted for 86000s in identical geometrical cylinders. Self-absorption corrections were
jj,
calculated following (Cutshall et al.
1982).
The sedimentation rates were obtained
Sand (>63
~lIn)
content could be an influencing factor in the 210Pb(ex)distribution due to
the granulmetric th icken ing towards the top of the cores (Figure
2).
Thus, the 210
P
b(ex)was
normalized by the fine grained fraction. This was done since sand has little or no activity
and may distort 210Pbex distributions (Ravichandran et al. 1995). After correction, the log
profiles of
2I
oPb(ex) \vere almost linear between an apparently turibid surface layers of the
PAA profileand background or
210
Pb supported at specilic depths of both cores (Figure 3
(a and b)). Excess 210Pb counting'errors ranged between 8 and 16%, increasing towards
the bottom of the cores. Since the log profile of the 2IOPb(ex)were almost linear, steady
using the slope of the log-linear curve that excludes the apparently mixed superficial
layer in the PAA core until supported depths; GTA (y = -0.15x
+
5.65) (1'2= 0.89; n=14;
p< 0.05) from the surface to the 17 em mark; PAA (y = -0.16x
+
5.54) (/ = 0.89; n= 14;
p< 0.05) 3.5 to the
23
em interval. The CIC dating method implies that the SAR has been
consistent during the time span of the 210Pb dating method (Appleby and Oldfield 1992).
b
An SAR of 2.0 mm/year for the previous ~ 20 em or ~ 100 years was determined for the
T7~
"
, .
In recent OM deposited in the study areas. Typical stable mangrove forest sediments
n
cont8in a generally higher OM contents in the surface sediments. In relation to
that this region may be going throLlgh modifications in the quantity and/or type of OM
being deposited. This has been taken in context with the opposing sedimentation
frequently separated by sand accumulation during intervening phases (Baltzer et al.
2004), we assert that the SAR in these region may not be keeping pace with the RSL rise
and that marine plankton and sand are slowly replacing mangrove debris and mud «63
~lm) deposition. The change in the sediment regime appears to be slow enough not to
have caused dramatic mangrove mortality but perhaps fast enough to cause an eventual
landward shift in the mangrove forest margins of this region. Such shifts have been
sea level further north is rising at a greater pace, indicated by 50 year tide gauge records
(near 4 cm/year, University of Hawaii http://www.soest.hawaii.eclu/UHSLC/, run through
the NIMED program), the assertion that the RSL rise is outpacing the SAR may be
expected. Shore line shifts and mangrove migrations, as indicated my sediment regimes,
may be particularly significant in places where tide gauges or aerial photographs have not
been used for periocls of time sufficient to determine sea level trends.
••
T
! 1'·,',',
I
!,
I
i:
,
"
: i
~,
.~ We would like to acknowledge the Instituto de Radioprote9ao e Dosimetria (lRD) for
Alongi, D.M., 2008. Mangrove forests: Resilience, protection from tsunamis, and
responses to global climate change. Estuarine, Coastal and Shelf Science 76, 1-13.
Alongi, D.M. et. aI., 200 I. Organic carbon accumulation and metabolic pathway in
sediments of mangrove forests in southern Thailand. Marine Geology 179, 85-
103.
Appleby, P.G., Nolan, PJ., Oldfield, F., Richardson, N. and Higgitt, R., 1988. Pb-210
dating of lake sediments and ombrotrophic peats by gamma essay. The Science of
the Total Environment 68, 157- 177.
Appleby, P.G., and Oldfield, F., 1992. Application of lead-21 0 to sedimentation studies,
p. 731-783. In M. Ivanovich and S. Harmon [eds.], Uranium Series
Disequilibrium: Application to Earth, Marine and Environmental Science. Oxford
Science Publications.
Baltzer, F., Allison, M., and Fromard, F., 2004. Material exchange between the
continental shelf and mangrove-fringed coasts with special reference to the
Amazon-Guianas coast. Marine Geology 208, 115-126.
Cahoon, D.R" and Lynch, CJ., 1997. Vertical accretion and shallow subsidence in a
mangrove forest of Southwerstern Florida, U.S.A. Mangroves and Salt Marshes 1,
173-186.
Chen, R., and Twilley, R.R., 1999. A simulation model of organic matter and nutrient
accumulation in mangrove wetland soils. Biogeochem istry 44, 93-118.
Cohen, M. C. L., Behling, H. and Lara. R.
J.,
2005. Amosonian Mangrove dynamics
during the last millennium: The relative sea-level and Little Ice Age. Review of
Palaeobotany & Palynology 136, 93-108.
Cutshall, N.H., Larsen, I.L. ancl Olsen. C.R., 1982. Direct Analysis of
21
oPb in Sediment
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Figure
1.
Study area (Paranag(j~ Bay and Guaranatuba Bay) Parana, Brazil.
Figure 2. Sand (>63~m) profile (dry wt
%)
vs depth.
Figure 3. Mud _normalized 210pbexdistribution for sediment cores; (a) GTA and (b)
PAA, in the format used for SAR calculations.
Figure 4. OM profile (dry wt %) vs depth,
Table 1. Dry bulk density of each sample, along with chlorophyll-a and pheo-pigment
contents of both sediment cores in this study.
r
f, ~.~
'I~.··
I
••
,
Sand(%)
30 40 50
I
I
I
I
I
I
,
II
PAA
II
GTA
Figure 4.
5
0
5
,-.,
8
10
""
'-'
.=
-
Q"
'"
Q
15
20
Jlt
OM(%)
15 20
II
GTA
IllPAA
Table I.
'ft
Depth
PAA
GTA
Dbd
Clor-a10C
Pheo/O
C
Dbd
Clor-a10C
Pheo/OC
.lli!i
(cm)
(g1cm
3
)
(ug/g)
(ug/g)
(glcm
3
)
(ug/g)
(uglg)
A'
0- 1
0.51
i5.10
29.09
0.20
26.38
71.67
.
,
~,.
1 - 2
0.38
24.51
51.21
0.23
16.70
61.42
2-3
0.35
29.15
52.02
0.21
\6.17
53.67
3 - 4
0.36
19.79
47.03
0.23
11.38
31.92
4 - 5
0.40
12.38
41.81
0.23
10.25
35.73
5 - 6
0.41
13.61
24.88
0.23
9.3 \
35.14
6 - 7
0.43
8.33
25.74
0.24
6.32
29.83
7 - 8
0.37
7.\ I
30.40
0.24
7.23
23.58
8 - 9
0.39
6.94
38.29
0.25
6.59
25.09
9 - \0
0.37
7.94
27.68
0.24
7.01
24.50
\0 - \2
0.38
9.29
22.25
0.24
6.67
24.28
\2 - 14
0.35
4.\\
25.77
0.2\
\ \ .08
38.89
14 - 16
0.34
5.99
20.18
0.23
6.80
27.23
16 - \8
0.37
3.46
17.04
0.23
5.56
27.95
\8 - 20
0.38
6.84
13.60
0.22
5.55
31.77
20 - 22
0.33
7.95
24.85
0.2\
6.34
28.23
22 - 24
0.34
7.43
23.30
0.21
5.89
34.50
o Brasil possui uma grande quantidade de florestas de manguezais, 24,000 km
2
, em
relayao ao mundo inteiro, 160,000 km
2
.
Ja que os mangues sao conhecidos como areas que
estoca carbono organico (CO) (BOUILLON, et aI., 2008; ALONGI, 2008). Integrando os dados
lama ao longo da costa Brasileira, de 234 na Paranagmi para 1129 (g/m
2
/ano) de (CO)
i'la
292 (g/nl/ano). Vma significante indicac;ao de sete tese arelac;ao entre
0
estocagem de CO com
1
(2.3 TgCano-
l
) em relayao a taxa rnundial (18 TgCano-
l
) (BOUILLON, et ai., 2008). Com as
Nosso resultados indicam urn fluxo de 0.012 Bq cm
2
anol que e bem diferente da regiao
·'i'
localizado em Galveston, Texas, 0.0172 Bq cm
2
ano
l
(BASKARAN et aI., 1993) maissimilar
na area costeira de Tampa, Florida, onde valores de 0.012 Bq cm
2
anol foram medida
(BASKARAN e SWARZENSKI, 2006). Nos estudos do inventario de 210Pb e foco de sedirnento
trabalho inclui a medida de 210Pb pelo fallout vindo da chuva do Brasil. Com estes dados, os
inventario de 210Pb foi possivel ser calculado nas areas de estudo (Tabela 1), indicando a
l··.·:.~.·.··'.·.•·•.·
. l'
-
~.,
&
~':.
SAR (mm/year)
ove margin
;,riili&t1a}:';;;:
gm
'}~~E{M~~:' .,..,
*Media mundial; 292
(glm
/ano)*de carbono organico
da costa Brasileira neste estudo foram entre
1.8
e 2.8 mm a-I durante
0
seculo passado (Tabela
sedimentos. Carbono organico, nitrogenio total, fosforo, pigmentos,
0
l3
C (OC) e
015N
foram
A taxa de sedimentac;ao nas florestas de mangue varia entre 1,8
e
5,0
llli111ano.Enquanto na planicie de lama varia entre 4,0 e 7,3 mnllano ..
As florestasde mangue estao reagindo
0
aumentando do nive! do mar
local em de formas diferente. Algumas indicaam que estao mantend6 na
mesma posic;ao geogrifica (Ilha Grande e Cananeia) devido ao equilibrio
entre a taxa de acumula<;ao de sedimentos e
0
aumento no nivel do mar
enquanto outras mostram sinais de migra<;ao, em dire<;aoou continente
(Guaratuba e Paranagmi) e em dire<;aoao oceano (Tamandare).
As estratigrafias de marcadores organico com; TOC/TN, 8
13
C
co
C),
OP,
8
15
N e series de pigmentos, podem ser usado para indicar a fonte do
material depositado em ecossistemas de mangue atraves de tendencias e
contrastes
. As estratigrafias de marcadores geologicos como gronulometria e a
~
mineralogia podem ser usado para indicar a fonte do material depositado
em ecossistemas de mangue atraves de tendencias e contrastes
o carbono esta sendo estocado em grande quantidade nos ecossistemas de
mangue no norte do Brasil, onde os resultados indicam uma migrayao em
dire<;aoao mar e em menor quantidades no suI do Brasil, relativo
a
media
mundial, onde evidencia uma migra<;ao ao continente. Estes estocagens
indica uma das conseqiiencias de
lUn
provavel aumento no myel do mar
em rela<;aoao balanyo do carbono.
1:
',
,
~t
/
t
•.
'
'
.
. }
,
.1
·•·.•·..·
't:
,
i~
oc.
f·
:··
.,
..
,.
I
ii..•..•.......
~.
ci
:;.
I~
r..·.
~.,
"L
,.
.•..
.
,
I'
~
i
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