Dasar Ilmu Tanah Deskripsi Tanah

Foto: smno.kampus.ub.janu2013

DESKRIPSITANAH

BAHAN KAJIAN MK. DASAR ILMU TANAH. Smno.jursntnh.fpub.febr2013

DESKRIPSI TANAH

DIUNDUH DARI: http://en.wikipedia.org/wiki/Soil……. 13/2/2013

Soil is a natural body consisting of layers (soil horizons) that are primarily composed of minerals

which differ from their parent materials in their texture, structure, consistency, color, chemical,

biological and other characteristics.

It is the unconsolidated or loose covering of fine rock particles that covers the surface of the earth.

Tanah merupakan hasil akhir dari pengaruh iklim (temperature, precipitation), relief

(slope), organisme (flora dan fauna), bahan induk (mineral-mineral), dan waktu.

DESKRIPSI TANAH

DIUNDUH DARI: http://en.wikipedia.org/wiki/Pedology_%28soil_study%29……. 13/2/2013

Pedology (from Greek: πέδον, pedon, "soil"; and λόγος, logos, "study") is the study of soils in their natural environment.

It is one of two main branches of soil science, the other being edaphology.

Pedology mengkaji pedogenesis, morfologi tanah, dan klasifikasi tanah; sedangkan edaphology mengkaji cara-cara bagaimana tanah mempengaruhi tumbuhan, fungi,

dan organisme lainnya.

Soil is not only a support for vegetation, but it is also the zone beneath our feet (the pedosphere) of numerous interactions between climate (water, air, temperature), soil life (micro-organisms, plants, animals) and its residues, the mineral

material of the original and added rock, and its position in the landscape.

Selama proses genesisnya, profil tanah mengalami pendalaman dan mengembangkan lapisan-lapisan yang

khas, yang disebut 'horizon', sambil menuju keadaan kesetimbangan.

DESKRIPSI TANAH

DIUNDUH DARI: http://en.wikipedia.org/wiki/Soil_morphology……. 13/2/2013

SOIL MORPHOLOGY is the field observable attributes of the soil within the various soil horizons and the description of the

kind and arrangement of the horizons.C.F. Marbut championed reliance on soil morphology instead of

on theories of pedogenesis for soil classification because theories of soil genesis are both ephemeral and dynamic.

The observable attributes ordinarily described in the field include the composition, form, soil structure and organization of

the soil, color of the base soil and features such as mottling, distribution of roots and pores, evidence of translocated

materials such as carbonates, iron, manganese, carbon and clay, and the consistence of the soil.

The observations are typically performed on a soil profile. A profile is a vertical cut, two dimensional, in the soil and bounds

one side of a pedon. The pedon is the smallest three dimensional unit, but not less than 1 meter square on top, that

captures the lateral range of variability.

DESKRIPSI TANAH : HORISON

DIUNDUH DARI: http://soilsdev.waikatoregion.govt.nz/Topic-Describing_Soils/How_To_Recognise_Soil_Horizons/ ……. 16/2/2013

Horison tanah adalah lapisan-lapisan di dalam profil tanah yang posisinya sejajar dnegan permukaan tanah. A soil profile is made up of several horizons and each is distinguished from the horizon above or below by being different in one or more characteristics. These differences include colour, texture,

structure, consistence, and coatings.

MORFOLOGI TANAH

DIUNDUH DARI: soillab.ifas.ufl.edu/.../... ……. 13/2/2013

WARNATEKSTUR

STRUKTURDensity / PorositAS

PERGERAKAN AIRReactivity of mineral and organic colloids

KEMASAMAN TANAH & pH

Berdasarkan pada sifat fisika dan kimiawi :


MORFOLOGI TANAH

Color Dark/grayish-black color

Orange vs. Gray colors

Texture Sandy vs. Clayey

StructureGood vs. Poor Structure

Density Porosity, organic matter, compaction

Water Pore sizes, porosity, water movement, saturation

Reactivity Cation exchange capacity

Acidity Plant tolerances, buffering, base saturation


Factors Affecting Soil Formation

ClimateOrganisms/Vegetation

Parent materialTopography

Time

The 5 soil forming factors


Horison Utama - Master Horizons

1. O Organik

2. A Topsoil, Bahan organik, daur-ulang

3. E Elluviasi

4. B Berkembang /akumulasi

5. C Bahan induk tanah

6. R Batuan dasar

A horizon

B horizon

Horison C

O Horizon

PENAMAAN / PENGENALAN HORISON TANAH

E horizon

Organic matter

Sandy

Clays/iron

Parent


E horizon

A horizon

B horizon(Illuvial)

(Elluvial)

C horizon

R horizon

O horizon

Master Horizons; Horison Utama

B horizon

Enough information?


b – buried horizon – Horison terkubur c – concretions d – root restrictive g – gleying h – illuvial organic matter k – carbonates m – cementation o - oxic p – plowing/disturbance q – secondary silica r – soft bedrock (saprolite) s – illuvial sesquioxides and O.M. t – clay accumulation v – plinthite w – development of color/structure x - fragipan

Subordinate Distinctions


g – gleying h – illuvial organic matter p – plowing/disturbance t – clay accumulation w – development of color/structure o – oxic - Oksik

h = Akumulasi bahan organik

1. Akumulasi bahan illuvial kompleks logam-bahan organik2. Selimut pada pasir dan partikel diskrit3. h = “humik”4. Value dan chroma sekitar 3 atau kurang5. Digunakan dnegan horison utama B (mos. Horison Bh)

Horison Bh“Horison Spodik”

Subordinate Distinction


p = dibajak/diolah, plowedHorison permukaan yang terganggu (Kultivation, pasture, Kehutanan)Digunakan dengan horison utama A (mis. Horison Ap)

Ap horizon



t = akumulasi liat

1. Translokasi liat atau terbentuk di tempat2. Selimut atau diskrit3. Digunakan dnegan horison utama B (mis. Bt)4. Kalau reduksi, dapat digunakan dengan sub-horison g (Btg)

Pembeda sub-ordinat = Subordinate Distinction


w = warna atau struktur

Perkembangan warna atau struktur secara Non-illuvial“w” = “weak”

Biasanya digunakan dnegan horison utama B (mis. Bw)

Bw



o = oxic horizon

1. Aktivitas liat rendah2. Sedikit bahan dapat lapuk3. Struktur batuan sedikit4. Oksida Fe dan Al


Horison oksik mempunyai: 1. a CEC 7 < 16cmol(+)/kg of clay and an ECEC < 12 cmol(+)/kg of clay which is due to the low activity clay minerals (1:1 clays, Fe and Al oxides, etc)2. < 10% weatherable minerals in the sand fraction3. Struktur batuan < 5%


Subordinate Distinctions g – gleying h – illuvial organic matter p – plowing/disturbance t – clay accumulation w – development of color/structure o – oxic DIUNDUH DARI: soillab.ifas.ufl.edu/.../...

……. 13/2/2013

KEJELASAN - DISTINCTNESSDistinctness describes the ease with which

features can be identified. It is often used for mottle colour and surface coatings.

Faint:Features can only be identified using 10x lens and cannot be positively identified in all places. They

are generally thin and their contrast with the adjacent matrix is small.

Distinct:Features have sufficient colour or texture contrast to be seen without magnification, but may need a

lens for positive identification.

Prominent:Features are conspicuous without magnification and can be readily distinguished from the matrix

by sharp colour or texture contract or by their thickness. Some thin features, eg mangans can be

prominent.

Sumber: http://soilsdev.ew.govt.nz/Topic-Describing_Soils/Distinctness/

a, e, iMenyatakan derajat dekomposisi bahan

organik dalam Horison O

Oa – Dekomposisi lanjut (Saprik)Oe – Dekomposisi moderat (Hemik)Oi – Dekomposisi ringan (Fibrik)

Saprik – Dekomposisi lanjut, serat tumbuhan sedikit, kandungan air rendahHemik – Dekomposisi sedang / intermediateFibrik – dekomposisi ringan, serat-serat masih dapat dikenali



Ikhtisar

Horison Utama: O, A, E, B, C, R

Simbol Subordinate : g, h, p, t, w and a,e,i

Contoh: Oa, Oe, OiBtBgBtgBwAp


Vertical SubdivisionsDicirikan oleh sifat-penciri utama dan/atau subordinat yang serupa, dipisahkan oleh

“degree”.

Bt1

Bt2

Bt3

Horison Bt


Horison Transisi

Lapisan transisi di antara horison utama.

AEEBBE

Ciri Dominan

Ciri Subordinate


Order

Suborder

Great group

Sub group

Family

Series

12

19,000

Hierarkhi Taksonomi Tanah

63

250

1400

8000

KingdomPhylumClassOrder FamilyGenusSpecies


Unit-unit untuk klasifikasi tanah

Pedon – smallest three-dimensional unit that displays the full range of properties characteristic of a given soil. (1-10 m2 of area)

- Unit mendasar dari klasifikasi tanah

Polypedon – Sekelompok pedon yang berhubungan erat di lapangan

Soil Series – class of soils world-wide which share a common

suite of soil profile properties


Unit-unit Sampel Tanah

Malabar SeriesDIUNDUH DARI: soillab.ifas.ufl.edu/.../... ……. 13/2/2013

Horison Diagnostik (Horison Penciri) untuk Klasifikasi Tanah

Permukaan

Bawah-perrmukaan


Diagnostic Surface HorizonsEpipedon

MollikUmbrikOchrikHistik

MelanikPlaggen

Anthropik

DIUNDUH DARI: http://www.soils.wisc.edu/courses/SS325/organic.htm ……. 16/2/2013

http://www.soils.wisc.edu/courses/SS325/organic.htm

MollicHistik

Umbrik

Okhrik

Melanik

Plaggen

Anthropik

X

X

X

X

X = Florida

Horison-permukaan Diagnostik = Diagnostic Surface Horizons


Mollic Epipedon

Tebal > 18-25 cm

Warna Value < 3.5

lembab

Chroma < 3.5 lembab

C-organik > 0.6 %

Kejenuhan basa > 50 %

Struktur tanah Berkembang

sangat baikKarbon Organik = Bahan organik x 0.57


EPIPEDON UMBRIK

Memenuhi semua kriteria Epipedon Molik,Kecuali kejenuhan basanya < 50%

Secara kimiawi berbeda dengan Molik


EPIPEDON OKRIK = Ochric Epipedon

Terlalu : Tipis Ringan, warna terang Muskin bahan organik

Mollic

Umbric

Ochric = Pucat

Sangat umum - “Extremely common”


Epipedon Histik

1. Horison organik yg terbentuk di daerah basah

2. Warna hitam hingga coklat gelap

3. Bobot Isi rendah4. Tebalnya 20-30

cm

Organik = > 20% - 35% bahan organik. (Jenuh air, kadar liat )


Epipedon Melanik1. Sifatnya serupa dnegan

Molik2. Terbentuk dalam abu

vulkanik3. Ringan, Fluffy


Melanic Epipedon:

The melanic epipedon is a thick black horizon which contains high concentrations of organic matter, usually associated with short-range-

order minerals or aluminium-humus complexes. The intense black color is attributed to the accumulation of organic matter from which

"Type A" humic acids are extracted. This organic matter is thought to result from

large amounts of gramineous vegetation, and can be distinguished from organic matter formed

under forest vegetation by the melanic index.

(http://www.soils.wisc.edu/courses/SS325/organic.htm)

HORISON ANTHROPIK• Serupa dengan Molik (warna, bahan

organik)• Digunakan manusia• Tulang dan kerangka• Air dari aktivitas manusia


Anthropic Epipedon:

The requirements for the anthropic epipedon are the same for the mollic, except that P2O5 soluble in 1% citric

acid is > 250 ppm.


Epipedon PlaggenDihasilkan oleh penggunaan rabuk jangka panjang (100s tahun)

Horison permukaan buatan manusia, tua

Tebal > 50 cm


Plaggen Epipedon: The plaggen epipedon is a cultural surface horizon produced by long

continued manuring. Its color depends on the nature of the

manure. Commonly it contains artifacts, such as bits of bricks and

pottery through out its depth.


Diagnostic Surface Horizons

Epipedon:

MollicUmbricOchricHisticMelanicPlaggenAnthropic

Very common

Human-derived

“specialized”


Vegetasi

Akumulasi bahan organik

waktu

Akumulasi Bahan ORganik

Histic

Mollic, Umbric

ochric

Bahan induk

tmax = 3000 yrs


Diagnostic Subsurface Horizons

Clays Organic Matter Oxides

PembentukanTranslokasi

Transformasi


Horison-penciri yang lokasinya di bawah-permukaan

Endopedon (B)Agric : Akumulasi liat dan humus, akibat pengolahan tanahArgillic : Akumulasi liatCambic : "color" atau perkembangannya lemahKandic : Argillik dengan liat seperti-kaolinitNatric : Argillic, nilai ESP tinggiOxic : Pelapukan lanjutSombric : Masam, akumulasi humus, tropisSpodic : Masam, daerah dingin, akumulasi humus-sesquioxida

Bahan organik Liat Oksida

Smectit

Subsurface Horizons

Kaolinit

Juga: garam, karbonat, sulfida

Warna gelapLogam (Fe, Al)

IronAluminum

FormationTranslocation

Transformation



AlbicArgillicSpodic OxicKandicCambicSombricsulfuric

NatricAgricCalcic GypsicSalicDuripanFragipanPlacic

Sub-Horizon Designations




Horison Albik (putih)

Light-colored (Value > 6 moist )Elluvial (E master horizon*)Low in clay, Fe and Al oxidesGenerally sandy texturedLow chemical reactivity (low CEC)Typically overlies Bh or Bt horizons

albic

*tidak semua horion E adalah horison albik



Horison ArgilikAkumulasi liat silikat hasil iluviasiIlluvial based on overlying horizonJembatan liatSelimut liat



Accumulation based on absolute increases compared to relevant horizon above or below. Argillic horizon. An argillic horizon is an illuvial horizon in which layer-silicate clays have accumulated to a significant extent by

illuviation. They have formed below the surface of a mineral soil but may be exposed at the surface by erosion. In general, this is a B horizon which has an increase in clay content of at least 1.2 times that of the

eluvial horizon above and is, in general, parallel to the surface of the polypedon. This increase of 20% in clay content occurs most in soils within a vertical distance of less than 30 cm. In case of clayey soils, this

requirement would be unreasonable. If the surface horizon is greater than 40% clay, the increase of clay needed is only 8%. For sandy soils with less than 15% clay, an increase of 3% is required for meeting the

criteria of an argillic horizon. In other words, if the clay content of the eluvial horizon is between 15 and 40%, an increase in clay of 20% is needed to meet the requirements for an argillic horizon.


Horison Argilik Horison Kandik

Aktivitas liatTINGGI RENDAH

Iluviasi LiatPasti Belum tentu




Spodic Horizon

Spodik

1. Akumulasi bahan organik dan aluminum (+/- besi) hasil Iluviasi2. Berwarna gelap (value, chroma < 3)3. Kejenuhan basa rendah (masam)4. Terbentuk pada kondisi masam basah


Eluviasi (Horison E dan Horison A)

Bahan organik Liat

Spodic horizon

Bh horizon Bt horizon

Argillic horizon

Eluviasi dan Iluviasi

A

E

Bh

A

Bt

E



Oxic horizon

• Highly weathered (high temperatures, high rainfall)

- High in Fe, Al oxides- High in low-activity clays (kaolinite < smectite < vermiculite)

activity


DESKRIPSI TANAH

Sumber: Guidelines for soil description. Fourth edition. FOOD AND AGRICULTURE ORGANIZATION OF THE UNITED NATIONS. Rome, 2006

KARAKTERISTIK PERMUKAAN TANAH

Beberapa karakteristik permukaan tanah yang penting:

1. Singkapan batuan2. Fragmen kasar batuan3. Erosi tanah4. Kerak permukaan5. Retak permukaan6. Adanya garam7. Pasir putih8. Seresah tumbuhan9. Kotoran cacing10.Bongkahan/gumpalan11.Pelumpuran.

DESKRIPSI TANAH


Singkapan Batuan

Batuan-dasar yang tersingkap di

permukaan dapat mengganggu aktivitas

pertanian. Singkapan batuan ini dideskripsikan dalam bentuk persentase

tutupan permukaan, dan informasi lainnya

seperti ukurannya, tata-letaknya, dan

kekerasan batuan yang tersingkap.

Klasifikasi singkapan batuan

DESKRIPSI TANAH


Fragmen kasar di permukaan

Fragmen kasar ini termasuk

fragmen yang tersingkap sebagian,

dideskripsikan dalam bentuk

persentase tutupan

permukaan, dan ukuran fragmen.

Klasifikasi fragmen kasar di permukaan

DESKRIPSI TANAH


Erosi Tanah

Deskripsi erosi tanah harus difokuskan pada erosi tanah akibat aktivitas manusia. Biasanya sulit

membedakan antara erosi alamiah dan erosi yang dipercepat akibat manusia.

Erosi yang dipercepat merupakan akibat dari pengelolaan tanah yang “tidak tepat” , seperti

budidaya pertanian yang tidak tepat, overgrazing dan panen vegetasi alamiah yang berlebihan.

DESKRIPSI TANAH


Kategori Erosi

Erosi dapat dikelompokkan

menjadi erosi oleh air dan erosi oleh

angin, dan mencakup efek

eksternal (off-site) seperti sedimentasi

atau deposisi; kategori lainnya adalah gerakan

massa tanah (longsor dan

fenomena yang terkait).

Klasifikasi Kategori Erosi

DESKRIPSI TANAH


Luas area yang terpengaruh erosi

Total aera yang terpengaruh oleh

erosi dan sedimentasi/deposisi

diestimasi dengan kelas-kelas yang didefinisikan oleh

SOTER(FAO, 1995)

Klasifikasi luas area yang ada erosinya

DESKRIPSI TANAH


Derajat Erosi

It is difficult to define classes of the degree of erosion that would

be equally appropriate for all soils and environments and that would also fit the various types

of water and wind erosion. Ada empat kelas derajat erosi

yang direkomendasikan, dan ini harus dideskripsikan lebih lanjut, yaitu S (ringan), M

(moderat), V (parah), E (sangat parah).

For example, in the case of gully and rill erosion, the depth and

spacing may need to be recorded; for sheet erosion, the

loss of topsoil; for dunes, the height; and for deposition, the

thickness of the layer .

Klasifikasi derajat erosi

DESKRIPSI TANAH


Klasifikasi aktivitas erosi

Aktivitas erosi

Periode aktivitas erosi dan deposisi yang dipercepat dideskripsikan

menurut klasifikasi berikut:

DESKRIPSI TANAH


Kerak permukaan = Surface sealing

Kerak permukaan digunakan untuk mendeskripsikan adanya kerak yang berkembang di permukaan

ntanah setelah topsoil mengering. Kerak-kerak permukaan ini dapat menghambat

perkecambahan benih , menghambat infiltrasi air, dan meningkatkan runoff. Atribut kerak permukaan

adalah konsistensi (kering), dan tebalnya kerak.

Kerak permukaan yang tuidak menggulung seluruhnya pada saat mengering → Horison takyric.

Kerak permukaan → Hyperochric qualifier.

DESKRIPSI TANAH


Klasifikasi atribut kerak-permukaan

DESKRIPSI TANAH


RETAKAN DI PERMUKAAN

Retak-permukaan (Surface crack) berkembang pada tanah-tanah yang kaya tipe liat mengembang-kerut setelah

mengering. Lebarnya retakan ( lebar rata-rata atau rata-rata lebar dan lebar maksimum) di

permukaan diukur dengan satuan sentimeter. Rata-rata jarak di antara retakan juga diukur dengan satuan

sentimeter.

1. Retakan yang membuka dan menutup secara periodik → Vertisols.2. Retakan yang membuka dan menutup periodik , lebarnya ≥ 1 cm →

Ciri vertik.3. Retakan poligon yang dalamnya ≥ 2 cm kalau tanah mengering →

Horison takyric.

DESKRIPSI TANAH


Klasifikasi retakan permukaan

DESKRIPSI TANAH


Klasifikasi Garam di permukaan

Garam - SaltThe occurrence of salt at

thesurface may be

described in terms of cover, appearance and

type of salt.

Klasifikasi berdasarkan persentase tutupan

permukaan dan ketebalan.

Catatan untuk klasifikasi tanah:

Kerak terdorong oleh kristal garam → Puffic

qualifier.

DESKRIPSI TANAH


Klasifikasi karakteristik Pasir

Pasir = Bleached sand

The presence of bleached, loose

sand grains on the surface is typical for certain soils and

influences the reflection characteristics of the area and,

hence, the image obtainedthrough remote sensing.

Klasifikasi berdasarkan pada persentase tutupan

permukaan.

Batas-batas horison - HORIZON BOUNDARY


Batas-batas horison memberikan informasi tentang proses apa ayang dominan dalam genesis tanah. Dalam kasus-kasus tertentu, dampak antropogenik masa lalu terhadap bentang-lahan. Batas-

batas horison dideskripsikan dnegan indikator “kedalaman”, “kejelasan” dan “topografi”.

KedalamanMost soil boundaries are zones of transition rather than sharp lines of division.The depth of the upper and lower boundaries of each horizon is given in centimetres, measured from the surface (including organic and mineral covers) of the soil downwards.Precise notations in centimetres are used where boundaries are abrupt or clear. Rounded-off figures (to the nearest 5 cm) are entered where the boundaries are gradual or diffuse, avoiding the suggestion of spurious levels of accuracy. However, if boundary depths are near diagnostic limits, roundedoff figures should not be used. In this case, the depth is indicated as a medium value for the transitional zone (if it starts at 16 cm and terminates at 23 cm, the depth should be 19.5 cm).Most horizons do not have a constant depth. The variation or irregularity of the surface of the boundary is described by the topography in terms of smooth, wavy, irregular and broken. If required, ranges in depth should be given in addition to the average depth, for example 28 (25–31) cm to 45 (39–51) cm.

Catatan untuk klasifikasi tanah:Banyak horison penciri dan sifat-penciri ditemukan pada kedalaman tertentu. Batas kedalaman yang penting adalah 10, 20, 25, 40, 50, 100 dan 120 cm.

DESKRIPSI TANAH


Kejelasan dan TopografiKejelasan batas-horison

menyatakan ketebalan zone dimana batas horison belokasi

tanpa menjadi bagian dari salah satu horison terdekat.

Topografi batas-horison menyatakan “smoothness” variasi

kedalaman dari batas-horison.

Catatan untuk klasifikasi tanah1. Cryoturbation → cryic horizon,

Cryosols and Turbic qualifier.2. Tonguing of a mollic or umbric

horizon into an underlying layer → Glossic qualifier.

3. Tonguing of an eluvial albic horizon into an argic horizon → albeluvic tonguing and Glossalbic qualifier.

4. Diffuse horizon boundaries → Nitisols.

Klasifikasi batas horison, menurut kejelasan dan topografinya

DESKRIPSI TEKSTUR TANAH


Tekstur tanah menyatakan proporsi berbagai kelas ukuran partikel primer (atau separat tanah, atau fraksi tanah) dalam suatu volume tanah dan dideskripsikan sebagai Kelas Tekstur

Tanah. The names for the particle-size classes correspond closely with

commonly used standard terminology, including that of the system used by the United States Department of Agriculture (USDA). However, many national systems describing particle-size and textural classes use more or less the same names but different grain fractions of sand, silt

and clay, and textural classes.

KELAS TEKSTUR TANAH

Nama kelas tekstur (yang mendeskripsikan kombinasi kelas ukuran partikel primer) dari suatu tanah dinyatakan dnegan

kode-kode.In addition to the textural class, a field estimate of the percentage of

clay is given. This estimate is useful for indicating increases or decreases in clay content within textural classes, and for comparing field estimates with analytical results. The relationship between the basic textural classes and the percentages of clay, silt and sand is

indicated in a triangular form.

DESKRIPSI TANAH


Pembagian Fraksi PasirSands, loamy sands and sandy loams are subdivided according to the proportions of very coarse to coarse, medium, fine and very fine sands in the sand fraction. The proportions are calculated from the particle-size distribution, taking the total of the sand fraction as being 100 percent.

Estimasi Kelas Tekstur Tanah di LapanganThe textural class can be estimated in the field by simple field tests and feeling the constituents of the soil. For this, the soil sample must be in a moist to weak wet state. Gravel and other constituents > 2 mm must be removed.

Komponen yang mempunyai “rasa” berikut: 1. Clay: “soils finger”, kohesif (melekat), dapat dibentuk, plastisitas

tinggi dan mempunyai permukaan mengkilap setelah diremas (dipirit-pirit) di antara jari-jari tangan.

2. Silt: “soils finger”, tidak melekat, agak sulit dibentuk, mempunyai permukaan kasar setelah diremas di antara jari-jari tangan dan rasanya sangat bertepung (seperti bedak).

3. Sand: tidak dapat dibentuk, bukan “soil finger” dan rasanya sangat berbutir grainy.

TEKSTUR TANAH


Catatan untuk klasifikais tanah :Karakteristik diagnostik penting yang berasal dari kelas tekstur:1. Tekstur pasir berlempung atau lebih kasar hingga kedalaman ≥ 100 cm → Arenosol.2. Tekstur pasir halus berlempung atau lebih kasar dalam lapisan yg tebalnya ≥ 30 cm di

dalam 100 cm permukaan tanah → Arenic qualifier.3. Tekstur debu, lempung debu, lempung liat berdebu atau liat berdebu dalam lapisan

yang tebalnya ≥ 30 cm, di dalam 100 cm tanah permukaan → Siltic qualifier.4. A texture of clay in a layer ≥ 30 cm thick within 100 cm of the soil surface → Clayic

qualifier.5. ≥ 30 percent clay throughout a thickness of 25 cm → vertic horizon.6. ≥ 30 percent clay throughout a thickness of 15 cm → vertic properties.7. ≥ 30 percent clay between the soil surface and a vertic horizon → Vertisol.8. ≥ 30 percent clay, < 20 percent change (relative) in clay content over 12 cm to layers

immediately above and below, a silt/clay ratio of < 0.4 → nitic horizon.9. Sandy loam or finer particle size → ferralic horizon.10. A texture in the fine earth fraction of very fine sand, loamy very fine sand, or finer →

cambic horizon.11. A texture in the fine earth fraction coarser than very fine sand or loamy very fine sand

→ Brunic qualifier.12. A texture of loamy sand or finer and ≥ 8 percent clay → argic and natric horizons.13. A texture of sand, loamy sand, sandy loam or silt loam or a combination of them →

plaggic horizon.14. A higher clay content than the underlying soil and relative differences among medium,

fine and very fine sand and clay < 20 percent → irragric horizon.15. A texture of sandy clay loam, clay loam, silty clay loam or finer → takyric horizon.16. ≥ 8 percent clay in the underlying layer and within 7.5 cm either doubling of the clay

content if the overlying layer has less then 20 percent or 20 percent (absolute) more clay → abrupt textural change.

TEKSTUR TANAH


Catatan untuk klasifikais tanah :

Karakteristik diagnostik penting yang berasal dari kelas tekstur:1. An abrupt change in particle-size distribution that is not solely

associated with a change in clay content resulting from pedogenesis or a relative change of ≥ 20 percent in the ratios between coarse sand, medium sand, and fine sand → lithological discontinuity.

2. The required amount of organic carbon depends on the clay content, if the layer is saturated with water for ≥ 30 consecutive days in most years → organic and mineral materials.

3. The required amount of organic carbon depends on the texture → aridic properties.

4. The depth where an argic horizon starts depends on the texture → Alisols, Acrisols, Luvisols and Lixisols, and Alic, Acric, Luvic and Lixic qualifiers.

5. An argic horizon in which the clay content does not decrease by 20 percent of more (relative) from its maximum within 150 cm → Profondic qualifier.

6. Peningkatan absolut liat ≥ 3 % → Hypoluvic qualifier.7. Rasio Debu/Liat < 0.6 → Hyperalic qualifier.


Kunci Kelas Tekrtur Tanah

1. Tidak mungkin membuat gulungan (seperti kawat) diameter 7 mm (sekitar diameter pensil)1.1. not dirty, not floury, no fine material in the finger rills:• if grain sizes are mixed: unsorted sand US < 5• if most grains are very coarse (> 0.6 mm):• if most grains are of medium size (0.2–0.6 mm):• if most grains are of fine size (< 0.2 mm) but still grainy:• if most grains are of very fine size (< 0.12 mm), tending to be floury:

SandVery coarse & coarse sandMedium sandFine sand

Very fine sand

SCSMSFS

VFS

% liat

<5<5<5<5

<5

1.2. not floury, grainy, scarcely fine material in the finger rills, weakly shapeable, adheres slightly to the fingers:

Loamy sand LS <12

1.3. similar to 1.2 but moderately floury: sandy loam SL (clay-poor)

<10



2. Possible to roll a wire of about 3–7 mm in diameter (about half the diameter of a pencil) but breaks when trying to form the wire to a ring of about 2–3 cm in diameter, moderately cohesive, adheres to the fingers

2.1 very floury and not cohesive• some grains to feel:• no grains to feel:

2.2 moderately cohesive, adheres to the fingers, has a rough and ripped surface after squeezing between fingers and• very grainy and not sticky:• moderate sand grains:• not grainy but distinctly floury and somewhat sticky:

Silt loamSilt

Sandy loamLoamSilt loam

SiLSi

SLLSiL

<10<12

10-258-2710-27

2.3 rough and moderate shiny surface after squeezingbetween fingers and is sticky and grainy to very grainy:

Sandy clay loam SCL 20-35


Kunci Kelas Tekrtur Tanah3. Possible to roll a wire of about 3 mm in diameter (less than half the diameter of a pencil) and to form the wire to a ring of about 2–3 cm in diameter, cohesive, sticky, gnashes between teeth, has a moderately shiny to shiny surface after squeezing between fingers

3.1. very grainy:3.2. some grains to see and to feel, gnashes between teeth• moderate plasticity, moderately shiny surfaces:• high plasticity, shiny surfaces:

Sandy clay (Liat berpasir)

Clay loam (Lempung liat)Clay (Liat)

SC

CLC

35-55

25-4040-60

3.3. no grains to see and to feel, does not gnash between teeth• low plasticity:• high plasticity, moderately shiny surfaces:• high plasticity, shiny surfaces:

Silty clay loamSilty clay (Liat berdebu)Heavy clay Iliat berat)

SiCLSiCHC

25-4040-60>60



Catatan: Penentuan tekstur tanah di lapangan tergfantung pada komposisi mineralogis liat. Kunci-kunci yang disajikan di atas, terutama untuk tanah-tanah yang mengandung illite, chlorite dan / atau vermiculite. Liat Smectite lebih plastis, dan liat kaolinitik lebih lengket. Sehingga adanya liat Smektit dapat mengakibatkan overestimasi, dan adanya liat kaolinitik dapat mengakibatkan under-estimasi.

Source: Adapted from Schlichting, Blume and Stahr, 1995.

DESKRIPSI TANAH


Fragmen Batuan dan Artefacts

Keberadaan fragmen batuan dapat mempengaruhi status ketersediaan hara, pergerakan air, penggunaan dan pengelolaan tanah. Hal ini juga mencerminkan asal-usul dan tingkat perkembangan tanah.

Artefacts (sections on artefacts and description of artefacts [below]) are useful for identifying colluviation, human occupation, and industrial processes. Large rock and mineral fragments (> 2 mm) and artefacts are described according to abundance, size, shape, state of weathering, and nature of the fragments. The abundance class limits correspond with the ones for surface coarse fragments and mineral nodules, and the 40 percent boundary coincides with the requirement for the skeletic phase.

Kalau fragmen batuan tidak terdistribusi secara teratur di dalam suatu horison, tetapi membentuk semacam “stone line”, maka harus dinyatakan dnegan jelas.

DESKRIPSI TANAH


Kelimpahan (volume) fragmen batuan dan artefacts

DESKRIPSI TANAH


Ukuran fragmen batuan dan artefacts

Klasifikasinya disjaikan dalam tabel berikut.

Catatan untuk klasifikais tanah:Karakteristik penciri penting yang berasal dari jumlah fragmen batuan:1. < 20 percent (by volume) fine earth averaged over a depth of 75 cm

or to continuous rock → Leptosols and Hyperskeletic qualifier.2. ≥ 40 percent (by volume) gravel or other coarse fragments

averaged over:• a depth of 100 cm or to continuous rock → Skeletic qualifier;• a depth of 50–100 cm → Endoskeletic qualifier;• a depth of 20– 50 cm → Episkeletic qualifier.

3. ≥ 20 (volume) artefact dalam lapisan atas upper 100 cm → Technosols.

4. < 40 persen volume berupa kerikil atau fragmen kasar lain dalam semua lapisan hingga 100 cm atau horison petroplinthic, plinthic atau salic → Arenosols.

5. Material Fragmental, rongga-rongga di antara fragmen diisi oleh bahan organik → Histosols.

DESKRIPSI TANAH


Klasifikasi fragmen batuan dan artefact

DESKRIPSI TANAH


Klasifikasi bentuk fragmen batuanBentuk fragmen Batuan

Bentuk umum atau kebulatan fragmen batuan dapat

dideskripsikan sebagai: Pipih, Bersudut, Membulat, Bulat

(Rounded)

Catatan unt klasifikasi:Layers with rock fragments

of angular shape overlying orunderlying layers with rock

fragments of rounded shapeor marked differences in size

and shape of resistant minerals

between superimposed layers →

Diskontinyuitas litologis

DESKRIPSI TANAH


Kondisi pelapukan fragmen batuan dan

artefact

Kondisi pelapukan fragmen kasar

dideskripsikan sebagai F (Lapuk ringan), W (lapuk)

dan S (lapuk lanjut).

Catatan untuk klasifikasi tanah

A layer with rock fragments without weathering rinds

overlying a layer with rock fragments with weathering rinds →

lithological discontinuity.

Klasifikasi kondisi pelapukan fragmen kasar

DESKRIPSI TANAH


Sifat fragmen batuanSifat fragmen batuan dideskripsikan dengan menggunakan terminologi yang sama dnegan deskripsi tipe-batuan. Untuk fragmen mineral primer, dapat dipakai kode-kode lainnya.Fragments of individual weatherable minerals (e.g. feldspars and micas) maybe smaller than 2 mm in diameter. Nevertheless, where present in appreciablequantities, such fragments should be mentioned separately in the description. Forartefacts, see section on artefacts.

Catatan untuk klasifikasi tanah:Fragmen batuan yang tidak mempunyai sifat litologis sama dnegan batuan dibawahnya → lithological discontinuity.

DESKRIPSI TANAH


Derajat dekomposisi dan humifikasi gambut – peat

In most organic layers, the determination of the texture class is not possible. Morevaluable is an estimate of the degree of decomposition and humification of the organic material. Warna dan persentase jaringan tumbuhan aslinya pada bahan organik kering atau basah, dapat digunakan untuk estimasi derajat dekomposisinya.

Catatan unbtuk klasifikasi tanah:1. Histosol mempunyai lebih dari dua-pertiga (volume) jaringan

tumbuhan yang masih dapat dikenali → Fibric qualifier.2. Histosols have between two-thirds and one-sixth (by volume)

recognizable plant tissues → Hemic qualifier.3. Histosol mempunyai kurang dari seper-enam (1/6) (volume) )

jaringan tumbuhan yang masih dapat dikenali → Sapric qualifier.

DESKRIPSI TANAH


Estimasi lapang dan kode derajat dekomposisi dan humifikasi gambut - peat

DESKRIPSI TANAH


WARNA TANAH (MATRIX)

Warna tanah mencerminkan komposisi dan kondisi oksidasi-reduksi saat ini dan masa lalu yang dialami oleh tanah. Warna biasanya

ditentukan oleh penyelimutan partikel sangat halus bahan organik humik (warna gelap), oksida besi (kuning, coklat, orange dan merah), Oksida manganese (hitam) dan lainnya; atau ditentukan oleh warna

bahan induk tanah.

The colour of the soil matrix l of each horizon should be recorded in the moist condition (or both dry and moist conditions where possible) using

the notations for hue, value and chroma as given in the Munsell Soil Color Charts (Munsell, 1975). Hue is the dominant spectral colour (red,

yellow, green, blue or violet), value is the lightness or darkness of colour ranging from 1 (dark) to 8 (light), and chroma is the purity or

strength of colour ranging from 1 (pale) to 8 (bright). Where there is no dominant soil matrix colour, the horizon is described as mottled and

two or more colours are given.

Selain notasi warna, nama-nama warna baku Munsell juga harus diberikan.

DESKRIPSI TANAH


WARNA TANAH

For routine descriptions, soil colours should be determined out of directsunlight and by matching a broken ped with the colour chip of the

Munsell SoilColor Charts.

For special purposes, such as for soil classification, additionalcolours from crushed or rubbed material may be required. The

occurrence ofcontrasting colours related to the structural organization of the soil,

such as pedsurfaces, may be noted.

Where possible, soil colour should be determined under uniform conditions.

Early morning and late evening readings are not accurate. Moreover, the

determination of colour by the same or different individuals has often proved

to be inconsistent. Because soil colour is significant with respect to various soil

properties, including organic matter contents, coatings and state of oxidation or

reduction, and for soil classification, cross-checks are recommended and should

be established on a routine basis.

DESKRIPSI WARNA TANAH


Catatan untuk kalsifikasi tanah:

Intermediate colours should be recorded where desirable for the distinction between two soil horizons and for purposes of classification and interpretation of the soil profile. Intermediate hues (important for qualifiers, such as Chromic or Rhodic, and for diagnostic horizons, such as cambic) that may be used are: 3.5, 4, 6, 6.5, 8.5 and 9 YR.

Misalnya: 3.5 YR, berarti bahwa nilai intermediate-hue lebih dekat dengan nilai 2.5 YR daripada 5 YR; 4 YR berarti lebih dekat ke 5 YR, dst.

Kalau “value” dan “chroma” mendekati batas-batas diagnostik, tidak boleh dilakukan pembulatan nilai, tetapi pencatatan akurat harus dilakukan dnegan menggunakan nilai-nilai intermediate, atau dnegan jalan menambah tanda + atau tanda - .

Pentingnya diagnostik hue, value dan chroma:


1. Abrupt changes in colour not resulting from pedogenesis → lithological discontinuity.2. Redder hue, higher value or higher chroma than the underlying or an overlying layer → cambic

horizon.3. Hue redder than 10 YR or chroma ≥ 5 (moist) → ferralic properties, Hypoferralic and Rubic

qualifier.4. Hue 7.5 YR or yellower and value ≥ 4 (moist) and chroma ≥ 5 (moist) → Xanthic qualifier.5. Hue redder than 7.5 YR or both hue 7.5 YR and chroma > 4 (moist) → Chromic qualifier.6. Hue redder than 5 YR, value < 3.5 (moist) → Rhodic qualifier.7. Hue 5 YR or redder, or hue 7.5 YR and value ≤ 5 and chroma ≤ 5, or hue 7.5 YR and value ≤ 5

and chroma 5 or 6, or hue 10 YR or neutral and value and chroma ≤ 2, or 10 YR 3/1 (all moist) → spodic horizon.

8. Hue 7.5 YR or yellower or GY, B or BG; value ≤ 4 (moist); chroma ≤ 2 (moist) → puddled layer (anthraquic ).

9. Hue N1 to N8 or 2.5 Y, 5 Y, 5 G or 5 B → reductimorphic colours of the gleyic colour pattern.10. Hue 5 Y, GY or G → gyttja (limnic material).11. Chroma < 2.0 (moist) and value < 2.0 (moist) and < 3.0 (dry) → voronic horizon.12. Chroma ≤ 2 (moist) → Chernozem.13. Chroma ≤3 (moist) and value ≤ 3 (moist) and ≤ 5 (dry) → mollic and umbric horizon.14. Value and chroma ≤ 3 (moist) → hortic horizon.15. Value ≤ 4 (moist) and ≤ 5 (dry) and chroma ≤ 2 (moist) → plaggic horizon.16. Value > 2 (moist) or chroma > 2 (moist) → fulvic horizon.17. Value ≤ 2 (moist) and chroma ≤ 2 (moist) → melanic horizon.18. Values 4 to 8 and chroma 4 or less (moist) and values 5–8 and chromas 2–3 (dry) → albic

horizon.19. Lower value or chroma than the overlying horizon → sombric horizon.20. Value ≥ 3 (moist) and ≥ 4.5 (dry) and chroma ≥ 2 (moist) → aridic properties.21. Value ≤ 4 (moist) → coprogenous earth or sedimentary peat (limnic material).22. Value 3, 4 or 5 (moist) → diatomaceous earth (limnic material).23. Value ≥ 5 (moist) → marl (limnic material).24. Value ≤ 3.5 (moist) dan chroma ≤ 1.5 (moist) → Pellic qualifier.25. Value ≥ 5.5 (dry) → Hyperochric qualifier.

DESKRIPSI TANAH


MOTTLING : BECAK-BECAK

Mottles are spots or blotches of different colours or shades of colour interspersed with the dominant colour of the soil. They indicate that the soil has been subject to alternate wetting (reducing) and dry (oxidizing) conditions.Becak dideskripsikan dengan indikator “kelimpahan”, ukuran, kontras, batas, dan warna. Selain itu, “bentuk”, posisi, dan ciri-ciri lainnya juga dapat dicatat.

Catatan untuk klasifikais tanah:1. Mottles of oxides in the form of coatings or in platy, polygonal or reticulate

patterns are diagnostic for the anthraquic (plough pan), hydragric, ferric, plinthic and petroplinthic horizons and for the gleyic colour pattern.

2. Mottles of oxides in the form of concretions or nodules are diagnostic for the hydragric, ferric, plinthic, petroplinthic and, pisoplinthic horizons and for the stagnic colour pattern.

3. Redox depleted zones in macropores with a value ≥ 4 and a chroma ≤ 2 are diagnostic for the hydragric horizon.

4. Becak atau selimut yang berupa jarosite atau schwertmannite merupakan penciri untuk horison thionic dan Aceric qualifier.

5. Becak-becak berbentuk konsnetrasi kuning merupakan diagnostik (penciri) horison thionik.

DESKRIPSI TANAH


Warna Becak

Biasanya warna becak dideskripsikan secara umum

sesuai dengan Munsell Soil Color Charts.

Kelimpahan Becak

Kelimpahan becak dideskripsikan dalam “Kelas-kelas” yang menyatakan persentase

permukaan yang ditempati becak.

Batas-batas kelas sesuai dnegan nodul mineral.

When the abundance of mottles does not allow the distinction of a single predominant matrix or

groundmass colour, the predominant colours should be determined and entered as soil

matrix colours.

Klasifikasi kelimpahan becak-becak

DESKRIPSI TANAH


Ukuran Bercak

Kelas-kelas yang digunakan untuk menyatakan diameter

individual bercak.

Kelas-kelas ini sesuai dengan kelas-kelas ukuran nodul

mineral.

Klasifikasi ukuran becak

DESKRIPSI TANAH


Kontras BecakKontras warna antara

becak dan matriks tanah dapat dideskripsikan

sebagai Haint, Distinch, dan Prominent.

Batas BecakBatas antara becak dan matriks dideskripsikan sebagai “tebal” zone

transisi warna.

Klasifikasi ke-Kontras-an becak

Klasifikasi batas antara becak dan matriks

DESKRIPSI TANAH


SOIL REDOX POTENTIAL AND REDUCING CONDITIONSDetermination of redox potential by field method

Soil redox potential is an important physico-chemical parameter used to characterize soil aeration status and availability of some nutrients. The redox potential is also used in the WRB classification to classify redoximorphic soils.To measure redox potential (DIN/ISO Draft, DVWK, 1995), drive a hole into the soil using a rigid rod (stainless steel, 20–100 cm long, with a diameter that is 2 mm greater than the redox electrodes) to a depth about 1–2 cm less than the desired depth to be measured. Immediately clean the platinum surface of the redox electrode with sandpaper and insert the electrode about 1 cm deeper than the prepared hole. At least two electrodes should be installed for each depth being measured. After at least 30 minutes, measure the redox potential with a millivoltmeter against a reference electrode (e.g. Ag/AgCl in KCl of the glass electrode of pH measurements, installed in a small hole on the topsoil that has been filled with 1-M KCl solution). For dry topsoil, a salt bridge (plastic tube 2 cm in diameter and with open ends, filled with 0.5 percent (M/M) agar in KCl solution) should be installed in a hole beside and at the depth of the platinum electrodes. In this tube, the reference electrode should be installed.

The measured voltage (Em) is related to the voltage of the standard hydrogen electrode by adding the potential of the reference electrode (e.g. +244 millivolt at 10 °C of Ag/AgCl in 1 M KCl, +287 of Calomel electrode).For interpretation, the results should be transformed to rH values using the formula: rH = 2pH + 2Eh/59 (Eh in mV at 25 °C).

DESKRIPSI TANAH


Karakteristik Redoximorphic tanah dan hubungannya dnegan nilai rH dan proses-proses tanah

DESKRIPSI TANAH


Kondisi Reduksi

Reductimorphic properties of the soil matrix reflect permanently wet or at least reduced conditions. They are expressed by neutral (white to black:Munsell N1 to N) or bluish to greenish colours (Munsell 2.5 Y, 5 Y, 5 G, 5 B). The colour pattern will often change by aeration in minutes to days owing to oxidation processes.

The presence of FeII ions can be tested by spraying the freshly exposed soil surface with a 0.2-percent (M/V) α,α dipyridyl solution in 10-percent (V/V) acetic acid solution. The test yields a striking reddish-orange colour in the presence of Fe2+ ions but may not give the strong red colour in soil materials with a neutral or alkaline soil reaction. Care is necessary as the chemical is slightly toxic.

Catatan untuk klasifikasi tanah:An rH value of < 20 is diagnostic for reducing conditions in Gleysols, Planosols and Stagnosols, and stagnic and gleyic lower level units of other RSGs. Gaseous emissions (methane, carbon dioxide, etc.) are diagnostic for the Reductic qualifier.

DESKRIPSI TANAH


Pola warna Reductimorphic dan keberadaan senyawa Fe

DESKRIPSI TANAH


CARBONATES : KandunganKarbonat dalam tanah dapat berupa residu

bahan induk atau hasil bentukan baru (carbonate sekunder). Karbonat sekunde rterutama berbentu

bubuk halus kapur, selimut pada agregat, konkresi, kerak permukaan atau bawah

permukaan, atau “hard banks”. The presence of calcium carbonate (CaCO3) is

established by adding some drops of 10-percent HCl to the soil. The degree of effervescence of

carbon dioxide gas is indicative for the amount of calcium carbonate present. In many soils, it is

difficult to distinguish in the field between primary and secondary carbonates. Classes for the reaction of carbonates in the soil matrix are

defined as per Table xx. The reaction to acid depends upon soil texture and is usually more vigorous in sandy material than in fine-textured material with the same carbonate content. Other materials, such as

roots, may also give an audible reaction. Dolomite biasanya bereaksi lebih lambat dan

kurang kuat dibanding kalsit. Karbonat sekunder harus diuji secara terpisah; biasanya mereka ini

bereaksi lebih intensif dengan HCl.

Classification of carbonate reaction in the soil matrix

DESKRIPSI TANAH


Klasifikasi bentuk karbonat sekunder

Bentuk KarbonatThe forms of secondary carbonates in soils are

diverse and are considered to be informative for diagnostics of soil genesis. Soft carbonate

concentrations are considered to be illuvial, and hard concretions are generally believed to be of

hydrogenic nature.

Untuk Klasifikasi tanah:Pentingnya kandungan karbonat:1. ≥ 2 percent calcium carbonate equivalent →

calcaric material.2. ≥ 15 percent calcium carbonate equivalent in

the fine earth, at least partly secondary → calcic horizon.

3. Indurated layer with calcium carbonate, at least partly secondary → petrocalcic horizon.

4. 15–25 percent calcium carbonate equivalent in the fine earth, at least partly secondary → Hypocalcic qualifier.

5. ≥ 50 percent calcium carbonate equivalent in the fine earth, at least partly secondary → Hypercalcic qualifier.

6. Where a soil has a calcic horizon starting 50–10 cm from the soil surface, it is only a Calcisol if the soil matrix between 50 cm from the soil surface and the calcic horizon is calcareous throughout.

7. Calcisols and Gypsisols can only have an argic horizon where the argic horizon is permeated with calcium carbonate (Calcisols) or calcium carbonate or gypsum (Gypsisols).

DESKRIPSI TANAH


pH tanah di lapangSoil pH expresses the activity of the hydrogen

ions in the soil solution. It affects the availability of mineral nutrients to plants as well

as many soil processes. When the pH is measured in the field, the method used should be indicated on the field data sheet. The field

soil pH should not be a substitute for a laboratory determination. Field soil pH

measurements should be correlated with laboratory determinations where possible.In the field, pH is either estimated using

indicator papers, indicator liquids (e.g. Hellige), or measured with a portable pH meter in a soil suspension (1 part soil and 2.5 parts 1 M KCl or 0.1 M CaCl2 solution). After shaking the solution and waiting for 15 minutes, the pH value can be read. For the measurement, use a transparent 50-ml plastic cup with marks for 8 cm3 soil (~

10 g) and 25 ml solution.

Catatan untuk Klasifikasi Tanah

Pada kebanyakan tganah, nilai pH berkorelasi dnegan kejenuhan basa, hal ini penting dalam klasifikasi tanah di lapangan. Akan tetapi hal ini memerlukan pembuktian di laboratorium.

Klasifikasi nilai pH

DESKRIPSI TANAH


Kandungan Bahan organik tanah

“Bahan organik” refers to all decomposed, partly decomposed and undecomposed organic materials of plant and animal origin. It is generally synonymous with humus although the latter is more commonly used when referring to the well decomposed organic matter called “substansi humik”.

The content of organic matter of mineral horizons can be estimated from the Munsell colour of a dry and/or moist soil, taking the textural class into account. This estimation is based on the assumption that the soil colour (value) is due to a mixture of dark coloured organic substances and light coloured minerals.

This estimate does not work very well in strongly coloured subsoils. It tends to overestimate organic matter content in soils of dry regions, and to underestimate the organic matter content in some tropical soils. Therefore, the organic matter values should always be locally checked as they only provide a rough estimate.

DESKRIPSI TANAH


Estimasi kandungan BOT berdasarkan Munsell soil colour

DESKRIPSI TANAH


Kandungan BOT untuk klasifikasi tanah

1. If saturated with water for ≥ 30 consecutive days in most years (unless drained):• ≥ [12 + (clay percentage of the mineral fraction × 0.1)]% organic

carbon or• ≥ 18 percent organic carbon, else ≥ 20 percent organic carbon →

organic material.

2. Organic material saturated with water for ≥ 30 consecutive days in most years (unless drained) → histic horizon.

3. Organic material saturated with water for < 30 consecutive days in most years → folic horizon.

4. Weighted average of ≥ 6 percent organic carbon, and ≥ 4 percent organic carbon in all parts → fulvic and melanic horizon.

5. Organic carbon content of ≥ 0.6 percent → mollic and umbric horizon.

6. Organic carbon content of ≥ 1.5 percent → voronic horizon.

(Note: the ratio of organic carbon to organic matter is about 1:1.7–2.)Write the range or average value in the description sheet.

DESKRIPSI TANAH


STRUKTUR TANAH

Soil structure refers to the natural organization of soil particles into discrete soil units (aggregates or peds) that result from

pedogenic processes. The aggregates are separated from each other by pores or voids. It is preferred to describe the structure

when the soil is dry or slightly moist. In moist or wet conditions, it is advisable to leave the description of structure to a later time

when the soil has dried out. For the description of soil structure, a large lump of the soil should be taken from the profile, from

various parts of the horizon if necessary, rather than observing the soil structure in situ.

Sruktur tanah dideskripsikan dengan indikator “grade”, “ukuran” dan “tipe” agregat.

Kalau suatu horison tanah mengandung agregat dnegan bermacam “grade”, ukuran atau tipe, semuanya harus

dideskripsikan dan hubungan satu sama lain harus dijelaskan.

DESKRIPSI TANAH


DESKRIPSI TANAH


Grade StrukturIn describing the grade or

development of the structure, the first division is into apedal soils

(lacking soil structure) and pedal soils (showing soil structure).

In apedal or structureless soil, no aggregates are observable in place

and there is no definite arrangement of natural surfaces of weakness. Structureless soils are subdivided

into single grain and massive.

Single-grain soil material has a loose, soft or very friable

consistence and consists on rupture of more than 50 percent discrete

mineral particles. Massive soil material normally has a

stronger consistence and is more coherent on rupture. Massive soil

material may be further defined by consistence (below) and porosity

(below).

Klasifikasi struktur

DESKRIPSI TANAH


Klasifikasi Tipe Struktur

DESKRIPSI TANAH


Tipe Struktur

Tipe-tipe alamiah dari struktur tanah adalah

gumpal, pipih, granuler, dan lainnya.

Where required, special cases or combinations of

structures may be distinguished, which are subdivisions of the basic

structures.

Kode-kode yang direkomendaiskan

adalah seperti pada tabek berikut.

Kode tipe-struktur tanah

DESKRIPSI TANAH


Ukuran Struktur

Size classes vary with the structuretype. For prismatic, columnar andplaty structures, the size classesrefer to the measurements of the

smallest dimension of the aggregate.

Combined classes may beConstructed.

Where a second structure is present, its relation to the first structure isdescribed. The first and second

structures may both be present (e.g. columnar and

prismatic structures). The primary structure may break down into a

secondarystructure (e.g. prismatic breaking into

angular blocky). The first structure may

merge into the second structure (e.g. platy merging into prismatic).

Kelas ukuran kombinasi

Kombinasi struktur tanah

DESKRIPSI TANAH


Kelas-kelas ukuran untuk Tipe-tipe struktur tanah

DESKRIPSI STRUKTUR TANAH


Catatan untuk klasifikasi tanah:1. Soil structure, or absence of rock structure (the term “rock structure” also applies to

unconsolidated sediments in which stratification is still visible) in half of the volume or more of the fine earth → cambic horizon.

2. Soil structure sufficiently strong that the horizon is not both massive and hard or very hard when dry (prisms larger than 30 cm in diameter are included in the meaning of massive if there is no secondary structure within the prisms) → mollic, umbric and anthric horizons.

3. Granular or fine subangular blocky soil structure (and worm casts) → voronic horizon.4. Columnar or prismatic structure in some part of the horizon or a blocky structure with

tongues of an eluvial horizon → natric horizon.5. Moderate to strong, angular blocky structure breaking to flat-edged or nutshaped elements

with shiny ped faces → nitic horizon.6. Wedge-shaped structural aggregates with a longitudinal axis tilted 10–60 ° from the

horizontal → vertic horizon.7. Wedge-shaped aggregates → vertic properties.8. Platy structure → puddled layer (anthraquic horizon).9. Uniformly structured → irragric horizon.10. Separations between structural soil units that allow roots to enter have an average horizontal

spacing of ≥ 10 cm → fragic horizon.11. Platy or massive structure → takyric horizon.12. Platy layer → yermic horizon.13. Strong structure finer than very coarse granular → Grumic qualifier.14. Massive and hard to very hard in the upper 20 cm of the soil → Mazic qualifier.15. A platy structure and a surface crust → Hyperochric qualifier.16. Stratification in ≥ 25 percent of the soil volume → fluvic material.

DESKRIPSI TANAH


Konsistensi

Konsistensi mencerminkan derajat kohesi atau adhesi dari massa tanah. Konsistensi mencakup ciri-ciri tanah seperti

friability, plasticity, stickiness dan resistensi terhadap kompresi. Sifat ini sangat tergantung pada jumlah dan tipe

liat, bahan organik dan kandungan lengas tanah.

For reference descriptions, a recording of consistence is required for the dry, moist and wet (stickiness and plasticity) states. Where

applicable, the smeariness (thixotropy) and fluidity may also be recorded. For routine descriptions, the soil consistence in the natural moisture condition of the profile may be described.

Konsistensi basah selalu dapat dideskripsikan, dan kondisi lembab kalau tanahnya kering, dengan jalan menambahkan

air ke sampel tanah.

DESKRIPSI TANAH


Konsistensi pada kondisi

kering

Konsistensi kering

ditentukan dengan jalan

“memecah” atau “meremas”

massa tanah kering udara di

antara jari tangan “thumb and forefinger”.

Konsistensi massa tanah pada kondisi kering

DESKRIPSI TANAH


Konsistensi pada kondisi LEMBABConsistence when moist is determined by attempting to crush a

mass of moist or slightly moist soil material.

Konsistensi massa tanah pada kondisi lembab

DESKRIPSI TANAH


Konsistensi pada kondisi basah: Kelekatan maksimum dan plastisitas maksimum

Soil stickiness depends on the extent to which soil structure is destroyed and on the amount of water present. The determination of stickiness should be performed under standard conditions on a soil sample in which structure is completely destroyed and which

contains enough water to express its maximum stickiness.

In this way, the maximum stickiness will be determined and comparison between degrees of stickiness of various soils will be

feasible. The same principle applies to soil plasticity.

DESKRIPSI TANAH


Kelekatan Stickiness is the quality of adhesion of the soil material to other

objects determined by noting the adherence of soil material when it is pressed between thumb and Finger.

Klasifikasi kelekatan tanah

DESKRIPSI TANAH


Plastisitas tanahPlasticity is the ability of soil material to change shape continuously

under the influence of an applied stress and to retain the compressed shape on removal of stress. Determined by rolling the

soil in the hands until a wire about 3 mm in diameter has been formed

Klasifikasi plastisitas tanah

Deskripsi Konsistensi Tanah



1. Extremely hard consistence when dry → petrocalcic horizon.

2. Surface crust with very hard consistence when dry, and very plastic and sticky consistence when wet → takyric horizon.

3. Air-dry clods, 5–10 cm in diameter, slake or fracture in water within 10 minutes → fragic horizon.

4. Penetration resistance at field capacity of ≥ 50 kN m-1 → fragic horizon.

5. Penetration resistance of ≥ 450 N cm-2 → petroplinthic horizon.

http://saret.ifas.ufl.edu/publications/bsbc/chap6.htm

Soil consistency states for a sand and a clay soil (friable soil is best for tillage).



Deskripsi Tanah


Status lengas tanahSoil-water status is the term used for the moisture condition of a horizon at the time the profile is described. The moisture status

can be estimated in the field.


1. The definitions of mineral and organic materials and of the histic, folic and cryic horizons depend on the soil-water status.

2. Temporarily water-saturated → Gelistagnic, Oxyaquic and Reductaquic qualifiers.

3. Organic material floating on water → Floatic qualifier.4. Permanently submerged under water < 2 m → Subaquatic

qualifier.5. Flooded by tidewater, but not covered at mean low tide →

Tidalic qualifier.6. Artificially drained histic horizon → Drainic qualifier.

Deskripsi Lengas Tanah


Klasifikasi status lengas-tanah

Sumber: http://staff.aub.edu.lb/~webeco/SIM215soiltaxonomy.htm ....... 16/2/2013

Klasifikasi soil moisture regimes

Aquic : wet, anaerobic, mottledUdic : adequate water throughout yearUstic : Water may be deficient, but usually available during growing seasonXeric : Most moisture during the noncropping time, dry MediterraneanAridic : Long dry periods

http://staff.aub.edu.lb/~webeco/SIM215soiltaxonomy.htm

Deskripsi Bobot Isi (BI) Tanah


BOBOT ISI

Bulk density is defined as the mass of a unit volume of dry soil (105 °C). This volume includes both solids and pores and, thus, bulk density reflects the total soil porosity. Low bulk density values (generally below 1.3 kg dm-3) generally indicate a porous soil condition. Bulk density is an important parameter for the description of soil quality and ecosystem function. High

bulk density values indicate a poorer environment for root growth, reduced aeration, and undesirable changes in hydrologic function, such as

reduced water infiltration.

There are several methods of determining soil bulk density. One method is to obtain a known volume of soil, dry it to remove the water, and weigh

the dry mass. Another uses a special coring instrument (cylindrical metal device) to obtain a sample of known volume without disturbing the

natural soil structure, and then to determine the dry mass. For surface horizons, a simple method is to dig a small hole and fill it completely with

a measured volume of sand.

Field determinations of bulk density may be obtained by estimating the force required to push a knife into a soil horizon exposed at a field moist

pit wall.

Deskripsi BOBOT ISI Tanah


Estimasi Bobot Isi Tanah di Lapangan (Untuk tanah-tanah mineral)

Observasi Bentuk agregat tanah

Bobot isiKg/dm-3

Kode

Tanah-tanah berpasir, berdebu dan berlempung dnegan kandungan liat rendah

Many pores, moist materials drop easily out of the auger; materials with vesicular pores, mineral soils with andic properties.

Granular < 0.9BD1

Sample disintegrates at the instant of sampling, many pores visible on the pit wall. single grain, granular

0.9–1.2BD1

Sample disintegrates into numerous fragments after application of weakpressure.

single grain, subangular, angular blocky

1.2–1.4 BD2

Knife can be pushed into the moist soil with weak pressure, sampledisintegrates into few fragments, which may be further divided.

subangular and angular blocky, prismatic, platy

1.4–1.6 BD3

Knife penetrates only 1–2 cm into the moist soil, some effort required, sample disintegrates into few fragments, which cannot be subdivided further.

prismatic, platy, (angular blocky)

1.6–1.8 BD4

Very large pressure necessary to force knife into the soil, no furtherdisintegration of sample.

Prismatic > 1.8 BD5

Deskripsi BOBOT ISI Tanah


Estimasi Bobot Isi Tanah di Lapangan (Untuk tanah-tanah mineral)

Observasi Bentuk agregat tanah Bobot isiKg/dm-3

Kode

Tanah-tanah berlempung dengan kandungan liat tinggi, Tanah berliat

When dropped, sample disintegrates into numerous fragments, furtherdisintegration of subfragments after application of weak pressure.

Angular blocky 1.0-1.2BD1

When dropped, sample disintegrates into few fragments, further disintegration of subfragments after application of mild pressure.

Angular blocky, Prismatic, Platy, Columnar

1.2 -1.4BD2

Sample remains mostly intact when dropped, further disintegration possible after application of large pressure.

coherent, prismatic, platy, (columnar, angular blocky, platy, wedge– shaped)

1.4 -1.6 BD3

Sample remains intact when dropped, no further disintegration after application of very large pressure.

coherent (prismatic, columnar, wedge–shaped)

> 1.6 BD 4, 5

Note: If organic matter content is > 2%, bulk density has to be reduced by 0.03 kg dm-3 for each 1% increment in organic matter content.

Deskripsi Bobot Isi Tanah



1. Bobot Isi 0.90 kg dm-3 atau kurang → Ciri Andik.

2. Dalam tapak-bajak, bobot isi ≥ 20 percent (relative) lebih tinggi dari lapisan lumpur → Horison anthraquic.

Root penetration is not only limited by bulk density, but also by texture. Fine-textured soils contain fewer pores in size and abundance than needed for unrestricted root growth. Therefore, the evaluation of bulk density has to take soil texture into account.

Untuk keperluan evaluasi, juga dapat digunakan “packing density” (PD = BD + 0.009 ・% clay).

Source: according to Ad-hoc-AG-Boden, 2005.

Deskripsi Porositas Tanah


POROSITAS

Voids include all empty spaces in the soil. They are related to the

arrangement of the primary soil constituents, rooting patterns,

burrowing of animals or any other soil-forming processes, such as

cracking, translocation and leaching. The term void is almost equivalent to the term pore, but the latter is

often used in a more restrictive way and does not, for example, include

fissures or planes. Voids are described in terms of type, size and abundance. In addition, continuity,

orientation or any other feature may also be recorded.

Porositas merupakan indikasi total volume rongga yg dapat dikenali dnegan lensa pembesaran 10x,

diukur dengan areanya, dan dicatat sebagai persentase permukaan yang

dihuni oleh pori.

Klassifikasi Porositas

1 Very low < 2 %2 Low 2–5 %3 Medium 5–15 %4 High 15–40 %5 Very high > 40 %

Deskripsi Porositas Tanah


TypeThere is a large variety in the shapeand origin of voids. It is impractical

and usually not necessary todescribe all different kinds of

voids comprehensively. Emphasisshould be given to estimating thecontinuous and elongated voids.

The major types of voids may be classified in a simplified way. In most cases, it is recommended that only the size and abundance of the channels, which are mostly continuous tubular pores, be

described (Figure xx). For the other types of voids, the following size and abundance classes should serve as a guide for the

construction of suitable classes for each category .Klasifikasi Pori

I Inter-stitial

Controlled by the fabric, or arrangement, of the soil particles, also known as textural voids. Subdivision possible into simple packing voids, which relate to the packing of sand particles, and compound packing voids, which result from the packing of non-accommodating peds. Predominantly irregular in shape and interconnected, and hard to quantify in the field.

B Vesicular Discontinuous spherical or elliptical voids (chambers) of sedimentary origin or formed bycompressed air, e.g. gas bubbles in slaking crusts after heavy rainfall. Relatively unimportant in connection with plant growth.

V Vughs Mostly irregular, equidimensional voids of faunal origin or resulting from tillage or disturbance of other voids. Discontinuous or interconnected. May be quantified in specific cases.

C Channel Elongated voids of faunal or floral origin, mostly tubular in shape and continuous, varying strongly in diameter. When wider than a few centimetres (burrow holes), they are more adequately described under biological activity.

P Plane Most planes are extra-pedal voids, related to accommodating ped surfaces or cracking patterns.They are often not persistent and vary in size, shape and quantity depending on the moisturecondition of the soil. Planar voids may be recorded, describing width and frequency.


Charts for estimating size and abundance of pores

Deskripsi Pori Tanah


UKURAN PORIDiameter rongga-rongga yang

memanjang atau tubular dideskripsikan sebagai “sangat halus” hingga “sangat kasar”.

KELIMPAHAN PORIThe abundance of very fine and

fine elongated pores as one group,and of medium and coarse pores as

another group is recorded as thenumber per unit area in a square

Decimetre.

Catatan nuntuk Klasifikasi Tanah

1. Vesicular layer below a platy layer or pavement with a vesicular layer → yermic horizon.

2. Sorted soil aggregates and vesicular pores → anthraquic horizon.

Klassifikasi diameter pori

Klassifikasi Kelimpahan pori

FM = fine and medium; FF = fine and very fine; MC = medium and coarse.

Deskripsi Tanah


KONSENTRASI MATERIAL TANAH

Pengkayaan sekunder, sementasi dan re-orientasi.

SELIMUT = SELAPUT = Coatings

This section describes clay or mixed-clay illuviation features, coatings of other

composition (such as calcium carbonate, manganese, organic or silt),

reorientations (such as slickensides and pressure faces), and concentrations

associated with surfaces but occurring as stains in the matrix (“hypodermic coatings”). All these features are

described according to their abundance, contrast, nature, form and location.

Kelimpahan Selaput

For coatings, an estimate is made of how much of the ped or aggregate faces is covered. Corresponding criteria should be applied when the cutanic feature is related to other surfaces (voids, and

coarse fragments) or occurs as lamellae.

Kontras SelaputKlasifikasi konstras selimut seperti

berikut ini.

Klasifikasi kelimpahan selimut

Klasifikasi ke-kontras-an selimut

F Faint Surface of coating shows only little contrast in colour, smoothness or any other property to the adjacent surface. Fine sand grains are readily apparent in the cutan. Lamellae are less than 2 mm thick.

D Distinct Surface of coating is distinctly smoother or different in colour from the adjacent surface. Fine sand grains are enveloped in the coating but their outlines are still visible. Lamellae are 2–5 mm thick.

P Pro-minent

Surface of coatings contrasts strongly in smoothness or colour with the adjacent surfaces. Outlines of fine sand grains are not visible. Lamellae are more than 5 mm thick.

Deskripsi “Coating“ Tanah


SifatSifat selimut dapat

dideskripsikan seperti pada tabel berikut.

Bentuk SelimutFor some coatings, the form may be informative for their

Genesis. For example, manganese and iron–

manganese coatings of dendroidal form indicate their

formation owing to poor infiltration and periodically

reductive conditions because of percolating water.

Lokasi Selimut Lokasi selimut atau akumulasi

liat dijelaskan. For pressure faces and

slickensides, no location is givenbecause they are by definition

located on pedfaces.

Klasifikasi Sifat Selimut

C : Clay - LiatS : SesquioxidesH ; HumusCS : Clay and sesquioxidesCH : Clay and humus (organic matter)CC : Calcium carbonateGB : GibbsiteHC : Hypodermic coatings (Hypodermic coatings, as used here, are field-scale features, commonly only expressed as hydromorphic features. Micromorphological hypodermic coatings include non-redox features [Bullock et al., 1985].)JA : JarositeMN: ManganeseSL : Silica (opal)SA : Sand coatingsST : Silt coatingsSF : Shiny faces (as in nitic horizon)PF : Pressure facesSI : Slickensides, predominantly intersecting (Slickensides are polished and grooved ped surfaces that are produced by aggregates sliding one past another.)SP : Slickensides, partly intersectingSN : Slickensides, non intersecting

Source: Adapted from Schoeneberger et al, 2002.

Deskripsi Tanah



1. Evidence of silica accumulation, e.g. as coatings → petroduric horizon.

2. Slickensides → vertic horizon and vertic properties.

3. Evidence of clay illuviation → argic and natric horizons.

4. Cracked coatings on sand grains → spodic horizon.

5. Uncoated sand and silt grains → Greyic qualifier.

6. Clay coatings in the argic horizon → Cutanic qualifier.

7. Illuviation in the form of lamellae in the argic, natric and spodic horizon → Lamellic qualifier.

8. Coatings that have a different colour from the matrix.

Klasifikasi Bentuk Selimut

C ContinuousCI Continuous irregular (non-uniform,

heterogeneous)DI Discontinuous irregularDE DendroidalDC Discontinuous circularO Other

Klasifikasi lokasi selimut dan akumulasi liat

P PedfacesPV Vertical pedfacesPH Horizontal pedfacesCF Coarse fragmentsLA Lamellae (clay bands)VO VoidsBR Bridges between sand grainsNS No specific location

Deskripsi Tanah


Cementation dan Compaction

Keberadaan kompaksi atau sementasi dideskripsikan dnegan indikator “sifat”, “kontinyuitas”,

“struktur”, “agent danDerajat”.

Compacted material has a firmor stronger consistence whenmoist and a close packing ofparticles. Cemented material

doesnot slake after 1 hour of

immersionin water.

KONTINYUITASKlasifikasi kontinyuitas sementasi / kompaksi.

STRUKTURFabrik atau struktur lapisan sementasi atau kompaksi.

Klasifikasi kontinyuitas sementasi/ KompaksiB Broken The layer is less than 50 percent

cemented or compacted, and shows a rather irregular appearance.

D Discontinues The layer is 50–90 percent cemented orcompacted, and in general shows a regular appearance.

C Continues The layer is more than 90 percent cemented or compacted, and is only interrupted in places by cracks or fissures .

Klasifikasi fabrik lapisan semen/kompak

Deskripsi Tanah


Sementasi dan Kompaksi

NatureThe nature of cementation or

compaction is described according

to the cementing agent orcompacting activity.

DegreeKlasifikasi derajat sementasi /

kompaksi.

Klasifikasi sifat sementasi / kompaksiK CarbonatesQ SilicaKQ Carbonates–silicaF IronFM Iron–manganese (sesquioxides)FO Iron–organic matterI IceGY GypsumC ClayCS Clay–sesquioxidesM MechanicalP PloughingNK Not known

Klasifikasi derajat sementasi / kompaksi.

N : Non-cemented and non-compacted : Neither cementation nor compaction observed (slakes in water).

Y : Compacted but non-cemented Compacted mass is appreciably harder or more brittle than other comparable soil mass (slakes in water).

W : Weakly cemented : Cemented mass is brittle and hard, but can be broken in the hands.M : Moderately cemented : Cemented mass cannot be broken in the hands but is discontinuous

(less than 90 percent of soil mass).C : Cemented : Cemented mass cannot be broken in the hands and is continuous (more than

90 percent of soil mass).I : Indurated : Cemented mass cannot be broken by body weight (75-kg standard soil

scientist) (more than 90 percent of soil mass).

Deskripsi Sementasi / Kompaksi Tanah


Catatan untuk klasifikais Tanah:

1. Es ditutup oleh bahan organik → Histosols.2. Sementasi oleh es atau kristal es mudah dilihat → cryic horizon.3. ≥ 75 % es (volume) → Glacic qualifier.4. Sementasi oleh bahan organik dan aluminium → spodic horizon.5. Horison spodik sementasi → Ortsteinic qualifier.6. Iron pan that is 1–25 mm thick and is continuously cemented by a

combination of organic matter, iron and/or aluminium → Placic qualifier.7. Strongly cemented or indurated → petrocalcic, duric, gypsic and

plinthic horizons, Petric, Petrogleyic and Petrosalic qualifiers.8. Cementation on repeated wetting and drying → plinthic horizon.9. Roots cannot penetrate except along vertical fractures that have an

average horizontal spacing of ≥ 10 cm and occupy < 20 percent (by volume) of the layer → petrocalcic, petroduric and petrogypsic horizons.

10.Horison sementasi atu indurasi kuat yang terdiri atas bongkahan-bongkahan yang panjang horisontalnya < 10 cm → Fractipetric dan Fractiplinthic qualifiers.

11.Kompaksi alamiah atau artifisial → Densic qualifier.

Deskripsi Tanah


Konsentrasi Mineral

Konsnetrasi-mineral mencakup berbagai macam konsentrasi kristalin sekunder, microcrystalline dan

amorphous substansi non-organik sebagai pengisinya, Konkresi lunak, konsentrasi yang bentuknya tidak teratur

(becak-becak), nodul-nodul material yang terbentuk secara pedogenesis.

Gradual transitions exist with mottles (above), some of which may be considered as weak

expressions of nodules. The mineral concentrations are described according to their abundance, kind,

size, shape, hardness, nature and colour.

Deskripsi Tanah


Abundance (by volume)Kelimpahan konsnetrasi mineral

dapat diklasifikasikan seperti pada tabel.

Macam - JenisMacam-mavcam konsentrasi mineral dapat diklasifikasikan

seperti pada tabel.

Klasifikasi kelimpahan konsnetrasi mineral (volume)

N None 0 %V Very few 0–2F Few 2–5C Common 2–15M Many 15–40A Abundant 40–80D Dominant > 80

T CrystalC Concretion A discrete body with a concentric internal structure, generally cemented.SC Soft concretionS Soft segregation (or soft accumulation)

Differs from the surrounding soil mass in colour and composition but is not easily separated as a discrete body.N Nodule Discrete body without an internal organization.IP Pore infillings Including pseudomycelium of carbonates or opal.IC Crack infillingsR Residual rock fragment

Discrete impregnated body still showing rock structure.O Other

Deskripsi Tanah


Size and shapeUkuran dan bentuk konsentrasi

mineral.

HardnessKekerasan konsentrasi

mineral.

NatureKonsnetrasi Mineral

dideskripsikan sesuai dengan komposisi dan substansi yang

terkandung di dalamnya.

ColourThe general colour names are usually sufficient to describe

the colour of the nodules (similar to mottles) or of

artefacts.

Klasifikasi ukuran dan bentuk

Deskripsi Tanah


Warna konsentrasi mineral

WH White - PutihRE Red - MerahRS Reddish - KemerahanYR Yellowish redBR Brown - CoklatBS Brownish - KecoklatanRB Reddish brownYB Yellowish brownYE Yellow - KuningRY Reddish yellowGE Greenish - KehijauanGR Grey - KelabuGS Greyish BU Blue - BiruBB Bluish-black - Hitam kebiruanBL Black - HitamMC Multicoloured

Sifat konsentrasi mineral

Deskripsi “Konsentrasi Mineral”



1. ≥ 10 percent (by volume) of weakly cemented to indurated,2. silica-enriched nodules (durinodes) → duric horizon.3. Reddish to blackish nodules of which at least the exteriors are at

least weakly cemented or indurated → ferric horizon.4. Firm to weakly cemented nodules or mottles with a stronger chroma

or redder hue than the surrounding material → plinthic horizon.5. Strongly cemented or indurated reddish to blackish nodules →

pisoplinthic horizon.

Deskripsi Tanah: Aktivitas Biologis


AKAR - Roots

The recording of both the size and the abundance of the roots is in general

sufficient to characterize the distribution of roots in the profile. In specific cases,

additional information can be noted, such as a sudden change in root orientation.The abundance of roots can only be

compared within the same size class. The abundance of fine and very fine roots may

be recorded similarly as for voids , expressed in the number of roots per

decimetre square.

Ukuran - Size (diameter)Klasifikasi ukuran akar.

AbundanceKlasifikasi ekelimpahan akar.

Klasifikasi diameter akarVF Very fine < 0.5 mmF Fine 0.5–2M Medium 2–5C Coarse > 5Note: Additional codes are: FF, very fine and fine; FM, fine and medium; and MC, medium and coarse.

Kelimpahan akar

< 2 mm > 2 mmN None 0 0V Very few 1–20 1–2F Few 20–50 2–5C Common 50–200 5–20M Many > 200 > 20

Deskripsi Tanah


Aktivitas Biologis lainnya

Biological features, such as krotovinas, termite burrows, insect nests, worm casts and burrows of larger animals, are

described in terms of abundance and kind. In

addition, specific locations, patterns, size, composition or

any other characteristic may be recorded.

KelimpahanKeliimpahan aktivitas biologis dideskripsikan secara general.

Macam-Jenis-KindContoh-contoh aktivitas

biologis.

Kelimpahan aktivitas biologis

N NoneF FewC CommonM Many

Contoh Aktivitas Biologis

A ArtefactsB Burrows (unspecified)BO Open large burrowsBI Infilled large burrowsC CharcoalE Earthworm channelsP PedotubulesT Termite or ant channels and nestsI Other insect activity.

PROFIL TANAH - HIPOTETIK

Sumber: http://www.fao.org/Wairdocs/ILRI/x5546E/x5546e04.htm ……. DIUNDUH 16/2/2013

Tanah adalah lapisan tipis yang menutupi permukaan bumi , kecuali permukaan air dan singkapan batuan

yang terbuka.

Sifat dan ciri tanah ditentukan oleh faktor

lingkungannya. Lima faktor dominan dalam

genesis (pembentukan) tanah:

1. Ilkim2. Bahan induk (rocks and

physical and chemical derivatives of same),

3. Relief4. Organisms (fauna and

flora), 5. Waktu.

http://www.fao.org/Wairdocs/ILRI/x5546E/x5546e04.htm

Diunduh dari: http://blog.ub.ac.id/mastertommy/files/2013/01/panduan_deskripsi.pdf …. 13/2/2013

DESKRIPSI TANAH

………. Selanjutnya ….….

Dasar Ilmu Tanah Deskripsi Tanah

Documents

Transcript of Dasar Ilmu Tanah Deskripsi Tanah