.. THE PEAT GENESIS IN THE LOWLANDS OF CENTRAL KALIMANTAN PROVINCE. THE RESPECTIVE INFLUENCE OF PODZOLISATION AND BAD DRAINAGE, THE TWO MAIN PROCESSES'OF PEAT GENESIS IN KALIMANTAN. G. . SIEFFERMA"*, S. TRIUTOMO**, M.T. SADELMAN***, A. KRISTIJONO** S.A. * t* *** PARHADIMULYO**. . . ORSTOM - GADJA~I MADA UNIVERSITY programme of cooperation, Sekip K 3, Yogyakarta, DIY: Agency for the Assessment and Application of. Technology, (BPP Teknologi) J1. MH. Thamrin 8, Lt. 18, Jakarta. BAPPEDA, J1. Diponegoro 60, Palangka-Ra,ya, ,KALTEN&. / A B S T R A C T This study conce'rns numerous peat profiles of CENTRAL KALI- MANTAN P R O V I N C E , . l o c a t e d north and south of PALANGKA-RAYA, main- ly between KATINGAN and KAHAYAN 'rivers , along 2he SEBANGAU val- b ley. % . After a short presentation of the geomorphologic, climatic and geologic characteristics of the region, the distribution of the peat is studied. In the upper part of-the SEBANGAU valley, north and south ' of PALANGKA-RAYA, the peat is very often more than 4 meters thick, even in the highest topographic positions, and frequently associated with tropical podzcls. In the central and coastal part of the SEBANGAU valley the thickness of the peat usually does not exceed 1 meter. The peat accumulation has been interpreted by the authors C. ORS7'0ii:1 Funas Documentaire
Transcript
. . THE PEAT G E N E S I S I N THE LOWLANDS O F CENTRAL KALIMANTAN P R O V I N C E .
THE R E S P E C T I V E INFLUENCE O F P O D Z O L I S A T I O N AND BAD DRAINAGE,
THE TWO MAIN PROCESSES'OF P E A T G E N E S I S I N KALIMANTAN.
G . . S I E F F E R M A " * , S. TRIUTOMO**, M.T. SADELMAN***, A. K R I S T I J O N O * *
S . A .
*
t*
* * *
PARHADIMULYO**. . .
ORSTOM - G A D J A ~ I MADA UNIVERSITY programme of coopera t ion ,
S e k i p K 3 , Yogyakarta, DIY:
A g e n c y for t h e A s s e s s m e n t a n d A p p l i c a t i o n o f . Technology,
(BPP T e k n o l o g i ) J1. MH. Thamrin 8 , L t . 18, Jakarta.
BAPPEDA, J1. D i p o n e g o r o 6 0 , P a l a n g k a - R a , y a , ,KALTEN&.
/
A B S T R A C T
T h i s s t u d y conce ' rns n u m e r o u s peat p r o f i l e s of CENTRAL K A L I -
MANTAN P R O V I N C E , . l o c a t e d n o r t h and s o u t h of PALANGKA-RAYA, main-
l y b e t w e e n KATINGAN a n d KAHAYAN ' r ivers , along 2he SEBANGAU val- b
l e y . % .
A f t e r a s h o r t p r e s e n t a t i o n of the g e o m o r p h o l o g i c , c l i m a t i c
a n d geologic charac te r i s t ics of t h e r e g i o n , t h e d i s t r i b u t i o n
of t h e peat i s s tud ied .
I n t h e upper p a r t o f - t h e SEBANGAU va l ley , n o r t h a n d s o u t h '
of PALANGKA-RAYA, t h e peat i s ve ry o f t e n more t h a n 4 meters
t h i c k , even i n t h e h i g h e s t topographic p o s i t i o n s , and f r e q u e n t l y
associated w i t h t r o p i c a l p o d z c l s .
I n t h e cen t r a l and coas ta l p a r t of t h e SEBANGAU v a l l e y t h e
t h i c k n e s s of t h e peat u s u a l l y does n o t exceed 1 m e t e r .
The peat a c c u m u l a t i o n has b e e n i n t e r p r e t e d by t h e a u t h o r s
C.
ORS7'0ii:1 Funas Documentaire
% i ! * 2
\ * (4 .
a s a . r e s u l t of two d i f f e r e n t p rocesses :
- I n t h e upper p a r t of t h e SEBANGAU v a l l e y and nea r PALANGKA-
RAYA, t h e p e a t accumulat ion seems t o be t h e consequence of
an extreme base d e s a t u r a t i o n of Al hor izons of podzols which
has led t o a dec rease of t h e m i c r o b i o l o g i c a l a c t i v i t y and con-
s e q u e n t l y t o t h e accumulat ion of t h e non-decomposed o r g a n i c
ma t t e r s .
The p o d z o l i s a t i o n appea r s , l n t h i s ca se , as a p rev ious -
and necessa ry process f o r t h e p e a t accumulat ion and g i v e s
an i n t e r p r e t a t i o n of t h e podzol hor izons under ly ing t h e p e a t .
- I n t h e c e n t r a l and c o a s t a l p a r t of t h e SEBANGAU v a l l e y , t h e
o r g a n i c m a t t e r accumulat ion can be r e l a t e d w i t h t h e bad d r a i -
nage of c l a y e y and f l a t low-lands n e a r t h e s e a l e v e l . The
s m a l l t h i c k n e s s of t h e p e a t could be t h e consequence of a
h i g h e r m i c r o b i o l o g i c a l decomposi t ion a c t i v i t y r e l a t e d t o
a h i g h e r base s a t u r a t i o n of th'e subs t ra tum. * \
z
I n bo th cases, t h e mecanism once i n i t i a t e d , under f o r e s t '
cover , cou ld o n l y con t inue t h e bad d r a i n a g e c o n d i t i o n s and t h e
accumula t ion .of o r g a n i c ' m a t t e r s .
\
c . . . - . ,. . ,. .*
. .
. .
I
. .
. I
Many areas of t h
' INTRODUCTION
C e n t r a l Kalimantan P r v i n r
are cover
3.
d
w i t h t r o p i c a l podzols and p e a t . Th'e p e a t c a n be found i n p o o r l y
d ra ined p o s i t i o n s as w e l l as i n t h e h i g h e s t s u b h o r i z o n t a l topo-
g r a p h i c a l s i t u a t i o n s . The podzols and p e a t were s t u d i e d i n t h r e e
d i f f e r e n i environmental s i t u a t i o n s . Fig. 1: - and 2
. Zone 1 - On t h e PALANGKA-RAYA s u r f a c e , a . s u b h o r i z o n t a l , sandy
q u a t e r n a r y l e v e l .
Zone 2 - I n t h e p o o r l y d r a i n e d cen t r a l and upper SEBANGAU v a l l e y .
Zone 3 - In t h e t i d a l i n f luenced lower Sebangau v a l l e y . .
THE REGION
- . CLIMATE
The climate. is e q u a t o r i a l , w i t h a mean a n n u a l p r e c i p i t a t i o n
of about 2800' "/years. The p e r i o d from June t o September i s ..,
l o c a l l y c a l l e d " d r y season" ; i n f a c t it is o n l y a p e r i o d of
h i g h e r p r o b a b i l i t y of drought p e r i o d s . Drought p e r i o d s longe r
than a week can occur any month of t h e year . 1
Temperatures are remarkably s tab le throughout t h e year .
Average annual tempera ture is 28°C and the' d i f f e r e n c e between
t h e monthly average of t h e " c o l d e s t " and " h o t t e s t " month is
about 1OC. Highest and lowest d a i l y t empera tu res r e g i s t e r e d
are r e s p e c t i v e l y 36OC and 21OC. Dai ly v a r i a t i o n s are g r e a t e r
d u r i n g drought p e r i o d s and range from 6 t o 9OC.
Redlative- humidi ty remains h igh throughout t h e y e a r and
r a r e l y drops under 80%.
' ..
..
SITUATION MAP D
.... ..:
:. 5 ' I .
a.. .. . . ..
a . ..e.
. ... e .
I ".. : :.! .. . :: ..: . . i.:
:: * . . . .:
'I
.. ...
Figure 1. Location map of the study area
THE R I V E R NETWORK
The r iver network i s shown i n F i g u r e 1. The KATINGAN and
KAHAYAN, are t h e main r ivers d r a i n i n g t h e area and n o u r i s h i n g
t h e c o a s t a l s ed imen ta t ion . D a t a concern ing t h e amount of sedi-
ments t r a n s p o r t e d by these two r i v e r s are n o t available. However
t h e a s p e c t of t h e water d u r i n g the r a i n y season i m p l i e s a subs- ’.
t a n t i a l s o l i d t r a n s p o r t . S t i l l , n e a r l y t h e t o t a l i t y of t h e s o l i d
t r a n s p o r t comes from areas o u t of f i g u r e 1, s i t u a t e d more n o r t h .
The s o l i d materials carried a long by these r ivers , from t h e i n -
land , are main ly q u a r t z g r a v e l s and sands , small f e l d s p a r s and
i l . l i tes , and k a o l i n i t i c clays mixed w i t h a l i t t l e amount of
i r o n hydroxydes. These sed iments a r e s p r e a d a l l o v e r t h e c o a s t a l
i n u n d a t i o n area by marine and t i d a l c u r r e n t s ’ i b u t w e have t o
mention t h a t t h e coastal sediments coming p a r t l y from t h e E a s t ,
from t h e KAPUAS and BARITO, c o n t a i n , i n a d d i t i o n t o the p receden t
m i n e r a l s , an impor t an t amount of I r o n c h l o r i t e , Montmor i l lon i te
I n t e r s t r a t i f i ed clays and I r o n Sulphurs .
The SEBANGAU w i t h ’ black waters , does n o t show any m i n e r a l
t r a n s p o r t - T h i s r iver i s no th ing more t h a n t h e o l d i n f e r i o r
KATINGAN v a l l e y , deserted by t h i s stream probab ly some 4000
y e a r s B.P. T h e consequence of t h i s change i s t h e e x c e p t i o n a l
w a t e r s t a g n a t i o n favorable f o r p e a t fo rma t ion i n what i s a c t u a l l y
t h e c e n t r a l and upper SEBANGAU v a l l e y , W e must a l s o mention t h a t
the SEBANGAU v a l l e y c o n t i n u e s with a submarine v a l l e y on more
t h a n 1 0 0 km under t h e Java sea, l i k e the Kahayan, B a r i t o and
Sampit. r ivers , o n l y t h e Kat ingan .does n o t show a similar sub-
marine p ro longa t ion .
_ _ _. ... I. ... . . . .~
c
3 2 4 Js 10 20 30Km
Figure 2. SOIL DISTRIBUTION
c 5
GEOLOGY
The l a r g e s t p a r t of f i g u r e 1 area c o n s i s t s of r e c e n t , most-
l y unconso l ida t ed , q u a t e r n a r y d e p o s i t s , showing sand l a y e r s ,
c l a y l e n s e s a n d levels of r o l l e d q u a r t z g r a v e l s . This sed imentary
material has been leveled t o a q u a t e r n a r y s u r f a c e by one o r seve-
s a l sea t r a n s g r e s s i o n s , some 5 0 . 0 0 0 y e a r s B . P . , b e f o r e t h e l a t e s t
g r e a t sea r e g r e s s i o n . .
This q u a t e r n a r y s u r f a c e of some 80 km l a r g e shows an Eas’t-
West e x t e n s i o n of n e a r l y 400 km. I n . h i s s o u t h e r n p a r t i t s a l t i -
t u d e i s s i t u a t e d between 35 and 65 meters and rises g e n t l y up
, in t h e North t o 150 meters o.s.1. a t t h e c o n t a c t w i t h t h e t e r t i -
ary b e l t . South-west of PALANGKA-RAYA t h e same s u r f a c e can b e
found i n several places on t h e SEBANGAU - KATINGAN watershed;
b u t t h i s s u r f a c e has never been observed s o u t h of BERENG-BENGKEL
on t h e SEBANGAU - KAHAYAN watershed.
A l l t h e r iver major v a l l e y s , SEBANGAU v a l l e y inc luded , form
a second more r e c e n t t opograph ic l e v e l , more o r less 1 5 meters
l o w e r t h a n t h e p receden t s u r f a c e .
Igneous acid rocks r a n g i n g from A l k a l i n e S y e n i t e s t o gra- ,
n i t e s form a 1 4 8 meters h i g h h i l l u n i t n e a r T A N G K I L I N G and t h e ..
153 meters h i g h ’ g u n u n g CINTA B E R A H I , on t h e s o u t h e r n p a r t of
t h e KATINGAN - SEBANGAU watershed.
S m a l l e r ou tc rops of s i m i l a r rocks can be found i n s i x ’ o t h e r
p l a c e s , E a s t of KASONGAN a n d South, and South-west of PALANGKA-
RAYA. Thus, t he , s u r f a c e of t h e s e r o c k s ou tc rops and t h e s o i l s
o v e r - l a y i n g them r e p r e s e n t less t h a n 1% of f i g u r e 1.
So, t h e c o l d appea r s as a main f a c t o r of bad decomposi t ion
of o r g a n i c matter and t h a t i s t h e r eason why p e a t accumula t ions
are so f r e q u e n t i n temperate c o l d and b o r e a l climates ; t h a t
i s a l s o t h e e x p l a n a t i o n why under a l l l a t k t u d e s t h e amount of
s o i l o r g a n i c matter i n c r e a s e s w i t h t h e a l t i t u d e . But t h i s f a c t o r .
d o e s n ' t p l a y . a n y r o l e i n t h e peat fo rma t ion of Kalimantan.
T h e second most import 'ant f a c t o r i n f l u e n c i n g t h e decomposi-
t i o n of t h e biomass is t h e temporary O Y permanent e x c e s s ' o f water
and t h e consequen t ly d e f i c i e n c y i n oxygen n e c e s s a r y f o r the decom-
p o s i t i o n of t h e o r g a n i c m a t t e r . Anyone knows t h a t most of the
t rop ica l p e a t s are l o c a t e d i n p o o r l y drained p o s i t i o n s .
Y e t , t o these t w o w e l l known main f a c t o r s , w e have t o add
t w o o t h e r s , less w e l l known, b u t a b l e t o p l a y a de te rminan t par t
. i n t h e i n i t i a l s t a g e s of a p e a t accumulat ion p rocess .
The f irst i s t h e a b i l i t y of o r g a n i c f r a c t i o n s t o react
w i t h s o i l s m i n e r a l s , t o b u i l t organo-mineral complexes i n which
t h e o r g a n i c component becomes more r e s i s t a n t t o b i o l o g i c a l de-
composi t ion. I t is sometimes e a s y t o p u t s u c h organo-mineral
complexes i n ev idence by s imple p e d o l o g i c a l a n a l y s i s : I n many
v o l c a n i c areas one can f i n d side by side s o i l s of d i f f e r e n t age
_ _ -_- - __
on i d e n t i c parent-material. For example i n t h e C e n t r a l Cameroon
h igh lands there are 20 meters t h i c k o x y s o i l s on one m i l l i o n years
o l d basalts nex t t o 3 meters th i ck younger s o i l s on 150.000 years
o l d basal ts , underb t he same v e g e t a t i o n , i n s i m i l a r e c o l o g i c a l
c o n d i t i o n s . (S ie f fe rmann, 1 9 7 3 ) . The o l d e r s o i l w i l l show you
a cumula t ive amount of 432 Tonnes of o r g a n i c matter per h e c t a r e
and the younger one' 729 Tonnes per hectare. T h e s t r o n g d i f f e r e n c e
i n o r g a n i c matter of t h e s e two s o i l types can n o t be imputed .to'
the v e g e t a t i o n , t h e c l ima te , ' t h e d r a i n a g e o r t h e t e x t u r e ; b o t h
s o i l s have a heavy c l a y e y t e x t u r e and a s i m i l a r i n t e r n a l d r a i n a g e .
I n t he younger s o i l t h e s t r o n g e r , c l a y bounded, o r g a n i c matter
i s more r e s i s t a n t and less b iodegradable . I n t h e o l d e r s o i l '
more o r g a n i c matter is decomposed t h a n i n ' t h e younger one, and
t h i s d e s p i t e o f a g r e a t e r d e s a t u r a t i o n . I n some cases, main ly i n
a l t i t u d e ' s i t u a t i o n s , t h i s p r o c e s s may induce water r e t e n t i o n , con-
d i t i o n s a n d can be the i n i t i a l s tage of a p e a t accumulat ion.
Organic matter accumulat ion can a l s o be induced by an exces-
~ sive d e s a t u r a t i o n . I n many t r o p i c a l and e q u a t o r i a l s i t u a t i o n s
t h e s o i l l i x i v i a t i o n th rough e x c e s s i v e r a i n f a l l s d u r i n g thousands
of years leads t o monomineral s o i l s w i t h upper h o r i z o n s o n l y
composed of q u a r t z s a n d , i n which t h e amount of l i f e i n d i s p e n s a b l e
major and trace e lements becomes n e a r l y zero . Such s o i l s are re-
. p r e s e n t e d i n t r o p i c a l and e q u a t o r i a l c o u n t r i e s by so called ''Tro-
p i c a l podzols" o r "Giant podzo l s " . I n t h e upper Ao hor i zons occur s .
" a ' slow accumula t ion of o r g a n i c matter, even i n w e l l d r a i n e d topo-
g r a p h i c p o s i t i o n s . The accumulat ion of o r g a n i c matter b e g i n s
here th rough a lack of t h e minimum amount of major and trace ele-
ments n e c e s s a r y f o r a normal m i c r o b i o l i g i c a l l i f e . T h i s p r o c e s s
once started can induce . i n t he h i g h e s t s u b h o r i z o n t a l topogra-
p h i c a l p o s i t i o n s a water logged o r g a n i c ho r i zon and s ta r t rap id ly
a p e a t accumulat ion.
.. . _ .
CONCLUSIONS
T h e m o s t impor tan t f a c t o r of p e a t accumulation i n C e n t r a l
Ka l iman tan is. t h e temporary o r pe rmanen t excess of water . T h e
p e d o l o g i c a l su rvey carried o u t i n t h e Palangka-Raya area has
'Shown t h a t b e s i d e s t h e b a s i n p e a t t h e r e a r e a l s o p e a t accumula-
t i o n s i n a 15 t o 20 meters h i g h e r p o s i t i o n ove r ly ing b u r i e d
t r o p i c a l podzols . T h e g e n e t i c r e l a t i o n s of t h e b u r i e d podzols
and t h e o v e r l a y i n g p e a t are shown. The p o d z o l i s a t i o n appears
as a p rev ious , much o l d e r , and necessa ry p r o c e s s f o r the accumu-
l a t i o n of t h i s type of "h igh" p e a t .
15
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