Transcript Document

ARCHITEKTUR
& SIFAT FISIKA TANAH
WARNA TANAH
Valuable clues to the nature of soil properties and conditions.
Munsell Colour Charts
Hue (colour)
Chroma (intensity)
Value (brightness)
Value and chroma are assessed from each hue page (p. 122).
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Faktor yg mempengaruhi warna tanah:
1. Kandungan BOT (Bahan Organik Tanah)
- darkness and masking of oxidation effects
2. Kandungan lengas (air) tanah (lebih gelap kalau basah)
3. Presence and oxidation state of Fe and Mn oxides
- Oxidized - iron oxides - red
- Reduced - greys and blues when iron reduced (gley)
Well-drained soils have more oxidized conditions.
Calcite gives whitish colour in semi-arid regions.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
TEKSTUR TANAH
TEKSTUR
Based on sand, silt and clay fraction (see earlier notes)
Effect of exposed surface area on other soil properties
1.
2.
3.
4.
Increases capacity to hold water
Nutrients and chemicals retained more effectively
Release of nutrients from weatherable minerals faster
Electromagnetic charges. Increases stickiness and aggregation.
Not a lot of clay/organics are required to impart these features
Best soils are usually those with relatively equal proportions of
the different soil texture classes.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
LUAS PERMUKAAN
Review: surface area higher for smaller clasts
384 cm2
1,536 cm2
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
TIPE MINERAL DAN FRAKSI TANAH
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SIFAT TANAH VS. UKURAN PARTIKEL
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Analisis Ukuran Partikel di Laboratorium
Metode Pipette & Metode Hydrometer
1. Treat soil (eg. with H2O2) to remove organic matter
Metode Pipette
2. Separate out the coarse fragments (gravel, coarse sand and
fine sand). Silt and clay fragments are washed into a
sedimentation cylinder.
3. Silt and clay suspension is stirred and allowed to settle
4. Clay fraction assessed using pipette at given depth
determined by Stokes Law (d is particle diameter)
V= kd2
t = h/(d2k)
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
a. Separating out the
sand fragments
b. Silt and clay
suspension
c. Weight of each
sand fragment is
determined
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Metode Hidrometer
2. Place measured quantity of soil in a stirring cup and mix
with deionized water and a dispersing agent
[eg.(NaPO3)6]
3. Transfer to settling cylinder, add deionized water to a
measured level (eg. 1L) and record the temperature of the
suspension.
4. Insert plunger and mix by pulling plunger up with short
jerks. Record the start time with second accuracy.
5. Gently insert the hydrometer and record its reading after
a set time (eg. 40 seconds). Correct for temperature.
Repeat 4&5 three times or more to get a good average.
6. After 3 hrs (less in our case), take another reading with
the hydrometer.
7. Calculate % sand, silt, and clay, and determine the soil
textural
classclasses.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER:
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
STRUKTUR TANAH MINERAL
Struktur Tanah Mineral
- aggregates or peds
- affects water movement, heat transfer, aeration and porosity
-affected by human action (logging, grazing, tillage, drainage,
manuring, compaction and liming)
1. Spheroidal (granular or crumb)
- most common in A Horizons
2. Plate-like
- most common in E Horizons
- due to compaction or inherited from parent material
3. Block-like
- common in B Horizons of humid regions
4. Prism-like
- common in B Horizons of arid and semi-arid regions
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
p. 134
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Granular peds
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Plate-like structure
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Angular blocky peds
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Struktur Prismatis (prisms roughly 3-5 cm across)
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Columnar peds
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Analysis of structure in the field
1. Type of peds
2. Relative size of peds (fine, medium, coarse)
3. Distinctness or development of peds (weak, moderate, strong)
*Difficult to assess when the soil is wet*
Soil Particle Density
Dp = Mass per unit volume of soil solids
Measured in Mg/m3
Particle density is not affected by pore space, because it does not
take them into account.
Mineral soils mainly in the 2.60 to 2.75 Mg/m3 range
Up to 3.00 Mg/m3 if minerals very dense (eg. magnetite, hornblende)
Organic matter has a much lower particle density (0.90-1.30 Mg/m3)
BOBOT ISI (BI) TANAH
Db = Mass per unit volume of dry soil
•Soil corers used to obtain known volume
without disturbance
•Soils are then dried and weighed
*Db includes both solids and pores*
•Bulk density is affected by soil porosity
•Highly porous soils have a low bulk
density
Sandy soils have a higher bulk density
(larger pores, but lower porosity overall)
than silty or clayey soils.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
•Well-sorted (poorly-graded) soils generally have lower bulk density
•Well-graded soils generally have higher bulk density
•Tightly-packed soils have higher bulk density
•A typical, dry medium-textured soil weighs 1250 Kg/m3 or 1.25 Mg/m3
Careful with your pick-up truck!
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Well-graded
Uniform-graded
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
High bulk density indicates:
•Poor environment for root growth
•Reduced aeration
•Reduced water infiltration and drainage
Human Practices Increasing Bulk Density
Vehicular traffic and frequent pedestrian traffic
•major impact on forest soils, which have low bulk density
Tillage
Loosens soil initially, but depletes organic matter, resulting in
higher bulk density
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Effect of Soil Compaction on Root Growth
1. Resistance to penetration (roots must push the particles
aside and enlarge the pore to grow if pore is too small)
Exacerbated by dryness due to increased soil strength.
2. Poor aeration
3. Slow movement of nutrients and water
4. Build-up of toxic gases and root exudates
Roots penetrate moist sandy soils most easily for a given bulk density
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Total Porosity
Particle density approximately 2.65 Mg/m3 for silicatedominated minerals.
Total porosity (%) = 100 - [(Db/Dp) x 100]
Porosity varies:
•25% in compacted subsoils
•60% or more in well-aggregated, undisturbed soils with
high organic matter content
•80%+ in organic soils (peat)
•Cultivation reduces pore space, organic matter content and
granulation
•Cropping reduces macropore space.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Tipe Pori & Bentuk
Packing pores (between primary soil particles)
Interped pores (shape depends on ped/granules)
Biopores (often long, narrow and branched; some are
spherical)
PACKING PORES
BIOPORES
INTERPED PORES
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Makropori vs. Mikropori
Macropores: 0.08mm to 0.5cm+
1. Allow ready drainage of water and air movement.
2. Penetrable by smallest roots and a multitude of
organisms.
3. Spaces between sand grains are macropores
4. This is why sandy soils have low total porosity but
rapid drainage (hydraulic conductivity)
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
•Interped pores are macropores found between peds and
granules.
•Biopores are macropores produced by roots, earthworms
and other organisms
•Biopores are very important for root growth and
infiltration in clayey soils.
Vertical Pore-Size Distribution
•Macropores most prevalent near the surface
•Micropores usually dominate at depth
Why?
1. Small aggregates are more stable than larger ones
2. More organic material near surface
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Vertical distribution
of pore size in three
distinct soils
(a) Sandy loam
(b) Well-structured silt loam
(c) Poorly-structured silt loam
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Organic matter stabilizes aggregates
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Micropores <0.08 mm
•Too small to permit air movement
•Water movement slow (usually filled with water)
•A high porosity soil can still have slow gas and water
movement if dominated by micropores.
•Water generally unavailable to plants (held too tightly)
•Reduces root growth and aerobic microbial activity
•Decomposition by bacteria very slow to near-zero in
smallest pores.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Factors Affecting Aggregate Formation and
Stability
(i) Physical-chemical Processes
(ii) Biological Processes
Physical-chemical Processes
of Aggregation
Flocculation
•
•
clumps of clay develop, called floccules
Two clay platelets come close
together; the cations of the layer
between them are attracted to
the negative charges on each
platelet.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Clay floccules and charged organic colloids form bridges
that bind to each other and to fine silt
•Clay domain: platelets are stuck together due to Ca2+,
Fe2+, Al3+ and humus.
This results in well-structured soils.
•Na+ has a weaker attraction to negative charges on clays,
so clays repel one another and remain dispersed.
This results in poorly-structured soils.
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Mengembang & Mengkerut – Tanah
•Upon drying, water is removed from within the
clays, so the clay domains move closer together
•Shrinkage results, with cracks along planes of
weakness (therefore, peds form)
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Proses Biologis yg mempengaruhi Agregasi
(1) Earthworms and termites (burrowing and moulding)
•Move soil, ingest it, and produce pellets or casts
•Plant roots also move soil particles
(2) Roots and fungal hyphae (stickiness)
•Exude sticky polysaccharides
•Soil particles and microaggregates bound into larger agglomerations
called macroaggregates
•Mycorrhizae secrete a very gooey substance called glomalin
N.B. Hyphae are tubular filaments making up the fungus
(3) Organic glues produced by microoganisms
•Bacteria also produce sticky polysaccharides in decomposed plant
residues
•The glues resist dissolution by water
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
Efek Pengolahan Tanah terhadap Agregasi
Jangka Pendek:
•Improvement in aggregation if done on moderately
dry soil
•Breaks up large clods, loosening soil and increasing porosity
•Incorporates organic matter into the soil
Jangka Panjang:
•Loss of aggregation
•Enhanced oxidation of organic material reduces aggregation
•Loss of macroporosity occurs if tillage is carried out in a wet
soil (puddled)
•Effect less pronounced where Fe & Al oxides plentiful
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
PUDDLED
WELL-AGGREGATED
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt
SUMBER: classes.uleth.ca/200801/geog3080a/SOILS%20PART%20II%202008.ppt