Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties
Holocene Black Sea basin sediments were formed in our opinion in happened geocatastrofic event on the border Pleistocene–Holocene (8–9 thousand years ago). As a result on the Upper Pleistocene lake sediments occur organogenic mineral (sapropel diatoms and coccolith) marine sediments. The charact...
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Відділення морської геології та осадочного рудоутворення НАН України
2011
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| Zitieren: | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties / D. Dimitrov // Геология и полезные ископаемые Мирового океана. — 2011. — № 1. — С. 5-19. — Бібліогр.: 35 назв. — англ. |
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| citation_txt | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties / D. Dimitrov // Геология и полезные ископаемые Мирового океана. — 2011. — № 1. — С. 5-19. — Бібліогр.: 35 назв. — англ. |
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| container_title | Геология и полезные ископаемые Мирового океана |
| description | Holocene Black Sea basin sediments were formed in our opinion in happened
geocatastrofic event on the border Pleistocene–Holocene (8–9 thousand years
ago). As a result on the Upper Pleistocene lake sediments occur organogenic
mineral (sapropel diatoms and coccolith) marine sediments. The characteristic
features of happened catastrophe is the occurrence of hydrogen sulfide charging
that conserved the organic matter and protect it from decomposition. Chemical
composition and properties of deep water organogenic mineral deposits give us
reason to Tip of the raw material as an integrated multi purpose and most notably
in agriculture.
Голоценові осади Чорноморської западини, на наш погляд, формувалися в умовах геокатастрофічних подій, які відбувалися на межі плейстоцену–голоцену (8–9 тис. р. тому). В результаті над верхньоплейстоценовими озерними осадами залягають органо-мінеральні (сапропелеві, діатомові та кокколітові) морські осади. Характерною рисою катастрофи, що відбулася, є виникнення сірководневого зараження, що законсервувало органічний матеріал і запобігло його розкладу. Хімічний склад і властивості глибоководних органо мінеральних осадів дають нам підставу рекомендувати їх у якості комплексної сировини багатоцільового призначення, і в першу чергу – в біоземлеробстві.
Голоценовые осадки Черноморской впадины формировались, по нашему мнению, в условиях геокатастрофических событий, произошедших на границе плейстоцена–голоцена (8–9 тыс. лет тому назад). В результате над верхнеплейстоценовыми озерными осадками залегают органо минеральные (сапропелевые, диатомовые и кокколитовые) морские осадки. Характерной чертой произошедшей катастрофы является возникновение сероводородного заражения, которое консервировало органический материал и предохранило его от разложения. Химический состав и свойства глубоководных органо-минеральных осадков дают нам основание рекомендовать их как комплексное сырье многоцелевого предназначения, и в первую очередь в области биоземледелия.
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SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 5
ПОЛЕЗНЫЕ ИСКОПАЕМЫЕ
© D. Dimitrov, 2011
Institute of Oceanology, Bulgarian Academy of Sciences, Varna
SAPROPELIC, DIATOMACEOUS AND COCCOLITH
SEDIMENTS (UNITS IB, IA) OF THE BLACK SEA
BOTTOM – GENESIS, COMPOSITION AND PROPERTIES
Holocene Black Sea basin sediments were formed in our opinion in happened
geocatastrofic event on the border Pleistocene–Holocene (8–9 thousand years
ago). As a result on the Upper Pleistocene lake sediments occur organogenic�
mineral (sapropel diatoms and coccolith) marine sediments. The characteristic
features of happened catastrophe is the occurrence of hydrogen sulfide charging
that conserved the organic matter and protect it from decomposition. Chemical
composition and properties of deep�water organogenic � mineral deposits give us
reason to Tip of the raw material as an integrated multi�purpose and most notably
in agriculture.
The Kalamitian – Vityazevian, Oldchernomorian, unit 2 (Ib) layers in the
deep parts of the sea are represented by the so called sapropelic sediments. The
term sapropel comes from the Greek saprós – rotten and pёlós – ooze and was
first used by R. Lauternborn in 1901 to designate sediments from lakes rich in
organic material and smell of hydrogen sulfide. Lithologically they are very
well separated along the contrasting erosive lower and transitional upper
boundary with unit 1a (fig. 1). Sometimes they make a transition from the
Neoeuxine Ic through a thin “intermediate” layer but in most cases they lie on
the erosive surface of unit Iс – carbonate ooze of the seekreide type.
There are also cases when the erosion goes too deep and the sapropels lie
immediately on formation 2 – black pelitic ooze with autogenous iron sulfides.
The colour of the sediments ranges from dark green to brown. The bulk density
of the sediments varies from 1,25 g/cm3 to 1,30 g/cm3. The organic matter in
the sapropels varies widely from 3–4 to 18–20%. There is a direct correlation
between the content of Corg. and the depth of the sea. The content of Corg. grows
with the increase of the depth
(fig. 2.).
The sapropels form a
single horizon with constant
thickness typical of the Black
Sea basin. Analogues of the
sapropels on the shelf and the
upper part of the continental
slope are the green aleurite�
pelitic oozes with accumulation
Fig. 1. Contrasting lithological
varieties on the borderline of Ia
(Unit 1) – Ib (Unit 2)
DIMITROV DIMITAR P.
6 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
of plant detritus and
decomposed shells of Mytilus
galloprovincialis. The transition
from aleurite�pelitic oozes to
sapropels is facial. The organic
matter in the sapropels is of
heterogenous origin. They are
composed primarily of
planktogenic organisms (about
80%) and continental organic
matter (20%). The planktonic
organisms are well preserved in
most cases under the conditions
of the hydrogen sulfide zone. The main components of the sapropels are the
dinoflagellate cysts, diatom algae, coccolithophorids, peridinea.
The main components of the sapropels are the dinoflagellate cysts, the
coccolithophorids, the peridinea. There are frequent occurrences of mass
concentrations of fish skeletons. We should also note the high biological
productivity of the phytoplankton reaching sometimes 50 g/m3 but does not exceed
0,7 g/m3 on average (Morozova�Vodyanitzkaya, 1954; Morozova�Vodyanitzkaya,
Belogorskaya, 1957; Сорокин, 1982; Moncheva, 1991, 1992; Moncheva, Velikova,
1999). The dinoflagellates and the diatom algae are particularly developed in the
sediments and most widespread in the sapropels are Peridinium triguestrum,
Rhizosolenia alata, Chaetoceras curvisaetus, Chaetoseras /Spores/ where the
latter species represent 70% of all diatoms in the sapropels. Fig. 1. shows the
leading complex of diatoms for the sapropels that is almost the same for the
Holocene. Analogical species of diatoms also occur in the suspended matter. The
admixture of terrigenous organic matter coming from the continent composes
up to 20% of the total volume of the organic matter and is represented by small
plant detriturs, spore�pollen grains and other matter. A typical reference layer
for the Black Sea is the coccolithophorid algae Braurudosphaera bugelowi.
The same reference layer affects the “intermediate” layer forming 2–3
interbeds with thickness of 2–5 mm fixing the foundation of the typical sapropel.
In one of the best studied drill columns located in the abyssal area at a depth of
2100 m (C�544) the lower part of the sapropel lies with an erosion layer above
the Neoeuxinian muds of the seekreide type (fig. 3.). The upper part of the
sapropel horizon and the beginning of the coccolith interbeds (interval 60–70
cm) is dated at about 5 thousand years.
The reference layer itself indicates the beginning of the inflow from the
Mediterranean as accepted by many researchers (Ross, Degens, 1974;
Shterbakov, 1978; Kuprin et al., 1984) whereas Georgiev (1984) insists that it
marks the beginning of the hydrogen sulfide contamination. The accumulation
Fig. 2. Distribution of Сorg. in
the sapropels depending on the
depth (Dimitrov, Velev, 1988)
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 7
of sapropels testifies to a biogenous sedimentation with catastrophic parameters.
The paleogeographic picture of the formation of biogenous sediments of such
exceptional scale would look like as follows:
· The climate warmed up sharply after a prolonged Wьrmian glaciations
fixed within the interval of 10–70 thousand years.
· The level of the World Ocean that was lower by 120–130 m than the
modern level 18–20 thousand years ago rose and the inflow of Mediterranean
Fig. 3. Cross�sections of deep sea organogenic mineral sediments
DIMITROV DIMITAR P.
8 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
water with salinity of 36–38‰ began through the Bosphorus threshold about
8 thousand years.
At that time the Black Sea was a lake with brackish to freshwater with
salinity of about 5–6 ‰ within the boundaries of the Neoeuxinian basin at
present�day depths of 90–120 m. The inflowing Mediterranean water about 8
thousand years ago (this event was fixed in С�544 fig. 3.) were more saline
and heavier, rich in biogenous components, filled the deep water valley and
mixed with the substantially less saline Black Sea water. The consequences of
this event were catastrophic for the flora and fauna and this triggered the
sedimentation of organogenic mineral oozes with thickness from 45–50 cm to
1–2 m (fig. 3, 4). The sapropels have different thickness in the different
morpholithological zones. They are often absent from the continental slope,
the slopes and axes of the underwater valleys due to active sliding processes.
They are better preserved in the flat places where their thickness reaches 45–
60 cm. The thickness of the sapropels is most substantial at the foot of the
continental slope, where they reach up to 2 m (fig. 3, 4). The processes of
redeposition and brecciation are strongly expressed at the foot of the
continental slope (Chochov, 1984; Velev, Dimitrov, Feier, 1992;). Brecciated
sapropel often occurs also in the abyssal area particularly around the craters
of mud volcanoes (Dimitrov, 1990) (fig. 3, 4).
Fig. 4. Lithologic cross�section and main physical and mechanical parameters of С�
194, (Dimitrov, 1990), the symbols are the same as in fig. 3
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 9
Particularly strong is the effect of the suspension currents formed in
submarine valleys creating a unique cone�like train at the foot of the slope and
in the abyssal bottom as well as various picturesque forms of the redeposited
material.
Generally, two types of sapropel are distinguished in the cross�sections
on the basis of the lithological data. The typical sapropels are micro�layered
dense brown�green sediments with “rubber�like” appearance and sectility by
layers. In most cases they are permeated by finely dispersed pelite terrigenous
mud with thickness of the layers up to 5–6 cm indicating a temporary change of
sedimentation conditions. The thickness of the so called typical sapropel is
widerly variable – from 15–20 cm to 1 m. The typical sapropels are covered by
an amorphous watered sapropel mass with thickness within 30–70 cm. The
binomial of the sapropels points to a change in the regime of sedimentaiton and
gradual loss of organic matter from bottom up.
The studies of the organogenic component of sapropels show that the
nanofossils with organic shell consist of pollen, spores and dinoflagellate cysts
(Filipova et al, 1989).
The major component of typical sapropels are the dinoflagellate cysts with
organic shells which are not dead fossils but stages of the life cycle of groups of
phytoplanktonic organisms (Pyrrophyta) and often exceed the amount of
coccoliths and diatomea. The sapropels comprise the typical marine euryhaline
species Lingulodinium machaerophorum and the acritarchs Cymatiosphaera
globulosa while their appearance indicates a catastrophic change in the
temperature of the Black Sea (Coolen et al., 2009). These species are dominant
also in the content of modern phytoplankton. Deuser (1974); Traverse (1978);
Filipova et. al. (1983) suggest that the sudden disappearance of the freshwater
species Spiniferites cruciformis, Testatodinium psilatum and the appearance
of marine microfossils is due to the catastrophic change in the salinity of the
basin. Кhrishev, Georgiev (1981) established a drastic change of the hydrological
and sedimentation regime of the shelf on the basis of the erosion effects on the
Pleistocene�Holocene boundary. According to them the Neoeuxinian sediments
and their continental analogues were were eroded as a result of the sudden inflow
of marine water before 6800 BР. The considerable hiatus of the shelf as well as
of the continental slope and the abyssal bottom is due exclusively to the
substantial erosion of sediments as a result of the catastrophe. The human
presence at that time is disclosed by the presence of cereal pollen such as
Centaurea cynua (corn�flower), Plantago lanceolata (narrowleaf plantain) и
Polygonum aviculare (common knotgrass) (Filipova�Marinova, 2003).
The mineral component of sapropel mud is represented by a polycomponent
mixture of clayey minerals. It is dominated by illite and montmorillonite and
smaller amounts of chlorites and kaolinite (Chochov, 1990).
They are sparsely dispersed with single grains of quartz, feldspar, volcanic
glass and others. The carbonate minerals are represented mainly by calcite with
low content of magnesium and by dolomite, calcite (Georgiev, 1984).
The studies of the distribution of heavy metals in the fraction 0,1–0,05
mm shows anomalous concentrations mainly in the distribution of pyrite�
markasite.
DIMITROV DIMITAR P.
10 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
The main sediment�forming product in sapropels is the minerals of the
pelite fraction that are the successors of the litute in the Neoeuxine basin
(Butuzova et al. 1975; Ruskova, Georgiev, 1985; Ivanov, Ruskova, 1986). At
the same time, the catastrophic increase in the biological productivity at the
beginning of the Holocene led to “dilution” of lutite with considerable amounts
of organic matter and formation of a new type of sediments – sapropels.
The content of organic matter is dominated by aliphatic and alicyclic
compounds (Vassoevich, 1986). Imprints as well as their mass accumulation of
oak leaves (Quercus) and hornbeam leaves (Carpinus betulus) are often found in
the sapropel layers which shows presence of continental organic matter in
sapropels. This is also evidenced by the admixture of structureless dispersed
autochthonic organic matter related to the humus. The latter is characterized
by high�molecular compounds of condensed and partially hydrated aromatic
compounds. This means that the organic matter in the sapropels is heterogenous
and consists of a mixture of alochthonic and autochthonic organic matter. It is
characterized by high content of easily hydrolyzed substances (12,7–31,7%),
bitumoids (2,3–3%), humic acids and relatively high content of insoluble organic
matter (56,3–58,1%) (Shterbakov et al., 1978).
The obtained data indicate high content (up to 19,407 мg/g) of amino acids
in the composition of sapropels which corresponds to 6,3% of the organic matter
(Shnyukov et al., 2003). Many organic compounds related to the normal and
isoprene carbohydrates such as pristine, phytane, alkanes, three� and
tetraterpenes, as well as carotenoids, carboxylic acids, fatty acids including
palmitinic acid, pigments of the chlorophyll group (pheophytin and chlorophyll)
were established in the sapropelic sediments. Most of them (vitamins,
antibiotics, hormones) are biologically active substances. Interbeds of
accumulated fish bones are very often found in the sapropels where the content
of Р2О5 reaches 2,15%, while its content in the overall sapropel mass is 0,12%.
The micro� and macrocomponents of the sapropels are very specific and
are a product of the interaction marine environment � hydrogen sulfide
contamination – organic and terrigenous component.
The concentrations of the main components (without Сorg.) varies widely:
SiO2 20–50%; SiO2amorph. – 0–10%; Al2O3 – 5–16%. The total amount of Si
and Al in the red clays, the sapropels and the coccolith oozes have a ratio of
1:0,55:0,23 while their amount in the terrigenous material has a ratio of
1:0,66:0,32 (Gavshin et al., 1988). A slight increase of the average content of
Na2O (2,05%), CO2 (1,98%), P2O5 (0,12%) is registered in the sapropel horizon.
The concentrations of Fe, Mn, Ti in the sapropels are close to their content in
the sediments lying below (Neoeuxinian – 1c) and above (Oldchernomorian and
present�day � 1a+1b)
There is some increase of the content of S�1% and Cl�2,04% in the
sapropels which is correlated to the content of Сorg.. All types of sapropelic
sediments have a stable content of more than 20 microelements. Some of them
(Mo, U, Cu, Zn, Ni, As, Se, Au, Ag and others) often exceed their clarke values
in the rocks, the sediments and the soils.
The geochemical features of the different types of sapropelic sediments
were established on the basis of the indicative ratios of the oxides: SiO2/
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 11
AL2O3, Na2O/K2O, FeO/Fe2O3 on the asis of the correlation analysis
(Blokhina, 1994).
The correlations of AL2O3 with K2O (0.96), MgO (0.81), Fe (0.54), indicate
the terrigenous origin of К, Mg and Fe, which migrate in the structure of the
silicates. The ratio SiO2/AL2O3 shows predominance of the terrigenous
sedimentation in the process of sapropel formation. The same is indicated by
the ratio Na2O/K2O that changes from 0,62 to 1,74. The lower values show a
higher degree of accumulation of the terrigenous component, and the higher
values – a leading role of the biogenous sedimentation.
What is typical of the sapropels in the western part of the Black Sea is the
dilution by clayey matter and the leading role of the pelite fraction. In conclusion,
it should be noted that the mineral composition of the clay component of the
sapropels is determined both by the type of the rocks feeding the western part
Fig. 5. Lithologic stratigraphic columns and distribution of Сorg. and carbonates in
DSOMS
DIMITROV DIMITAR P.
12 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
of the Black Sea and by the material delivered to the bottom by the mud
volcanoes.
No estimates have been made so far of the quantity of clayey material
delivered by volcano craters yet it could be assumed that its quantity is equal to
the quantity of clayey material coming from the land. The terrigenous and
endogenic component of the sapropels is a polycomponent mixture of clayey
minerals with predominance of illite and montmorillonite and lesser amounts
of chlorite and kaolinite. The comparison of the mineral composition of the
sapropels sediments with the mineral composition of the sediments lying above
them and below them shows that they are closer to the Neoeuxinian lutite than
to the diatom and coccolithophorid muds. The sharp rise in the importance of
the biogenous component in the sapropels serves as evidence of an ecological
catastrophe and a sudden increase in biological productivity. The sapropelic
sediments are a product of the dilution of exogenic and endogenic material mixed
with considerable quantities of dead biomass.
The organic matter in the sapropels is the majore sediment�forming factor
and comprises numerous micro and macrocomponents. The composition of the
organic matter differs from the composition of the layers lying above or below
by slightly higher content of easility hydrolyzable substances, bitumoids and
low content of insoluble residue (Velev, Dimitrov, Feier, 1992). The dispersed
amorphous organic matter is composed mainly of planktogenic organisms and
bacterioplankton and smaller quantities of continental organic matter.
The sedimentation process during the Holocene is determined by the same
factors and analogous sediment complexes that existed during the Karangatian,
the Paleogene and the Neogene. They are modern analogues of ancient sediments
such as the oil�bearing formations (facies “domanique”) (Velev, Dimitrov, Feier,
1992). In that sense they can serve as a model for reconstruction of the sediment
processes during the Cenozoic. The content of carbrohydrates in the sapropels
is similar to that of the oil�bearing rocks (Lopatin, Emets, 1987).
The distribution of organic matter in the cross�section of the sapropels
shows that the content of Сorg. is usually higher than that in rubber�like
sapropels (fig. 5).
There are also cases where the content of Сorg. in the upper part of the
cross�section is higher than in the middle or in the base. In such cases samples
are also taken from the common terrigenous interbeds. The analysis of the
current data of content of Сorg. in the cross�section of the sapropelic ooze s shows
stable high content of Сorg. in the typical dense stratified sapropels. The sapropel
horizon is steadily distributed throughout the water area of the basin as shown
on the lithofacial map of the Oldchernomorian sediments in unit Ib according to
Khrischev et al. (1988) where the facial diversity in the sapropels is well
reflected.
The chemical composition of the sapropelic sediments is sharply distinguished
from the composition of the underlying carbonate muds (seekreide type) and the
coccolith�carbonate Djemetinian muds lying above them. Their content of organic
matter varies in a wide range: from 2–3% to 18–20% (fig. 2, 5).
The distribution of organic matter during the different stages of the Upper
Pleistocene and Holocene, and more specifically in the Kalamitian sediments,
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 13
corresponds to the climatic conditions of the basin (fig. 2). The content of the
different components is shown in the table 1 and on fig. 6.
The table shows the considerable variation in the content of the different
components depending on the depth distribution of the mud and on the extent
of diagenetic changes. The content of sapropels in the Mediterranean (Shimkus,
1981) shows that they are much poorer in organic matter (1.5 – 10%, on average
– 5%) irrespective of the similar conditions of their formation.
The organic matter in the sapropels consists of a complex combination of
plant and animal products at a different stage of degradation and recombination.
Generally, they are divided into bitumoids, hydrolyzable substances, humic
substances and unhydrolyzable residue (kerogen).
The chloroform fraction of bitumoids is from 0,2 to 0,5% in dry matter.
The bitumoid fractions contain carbohydrates, esters, pigments, organic acids,
resins and asphaltens.
The production of chloroform bitumen on the basis of sapropels varies
within the boundaries 0,5–2,0% (per dry sample). The chemical composition of
the bitumen is the following (mean values): C � 7,3%; H � 10,85%; O2 � 10,9%;
N � 0,8%. The group components of the bitumoid are distributed in the following
way: oils � 19–35%; resins � 45–51%; asphaltens � 20–30% (Velev, Dimitrov,
Feier, 1992).
The infrared spectra of the bitumoids indicate that their carbon part
includes components with linear and branched carbon chains as well as cyclanes.
It is interesting that the aromatic carbohydrates are present in very small
amounts (traces). The range of normal alkanes comprises components with 14
to 34 carbon atoms and CPI within 1,6�3. The low�molecular carbon part of the
Table 1
Chemical content of DSOMS
(Dimitrov, Velev 1988; Velev, Dimitrov, Feier, 1992; Shnyukov et al., 1999)
Components
Content
(%, from – to)
Average
value (%)
Ñorg. 3–20 11,5
SiO2(total) 28–35 31,5
SiO2amorph 0–10 5
CaO 1–8 4,5
MgO 2,3–3,15 2,73
K2O 1.98–2.4 2,19
Na2O 2,05–2,07 2,06
Fe2O3 3,55–5,2 4,57
Al2O3 10,4–12,5 11,5
P2O5 0,12–0,38 0,25
TiO2 0,3–0,5 0,4
Chloroform
extract at 3%
content of Ñorg
0,2–0,5 0,35
Cu 0,01–0,05 0,03
Components
Content
(%, from – to)
Average
value (%)
Methanol–
acetone–
benzol
extract
0,02–0,04 0,03
Cr 0,01–0,015 0,0125
Mn 0,026–0,047 0,0365
Zn 0,0076–0,094 0,0085
Mo 0,013–0,022 0,0175
Co 0,013–0,018 0,0155
Ni 0,0065–0,0081 0,0073
Li 0,0021–0,003 0,00255
Sr 0,0027–0,0095 0,0061
V 0,0076–0,01 0,0088
Rb 0,013–0,02 0,0155
Se 0,0082–0,0086 0.0084
DIMITROV DIMITAR P.
14 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
N�alkanes is characterized by CPI values greater than 1. The maximum
concentrations of individual N�alkanes is С22, С25, С27, С29 and even С31. As a
whole the distribution of N�alkanes has highly variable configuration and often
has two or three peaks. The ratio between the isoprenoid components pristane
and phytane ranges broadly from 0,5 to 1,8 (Velev, Dimitrov, Feier, 1992).
The content of humic acids in the sapropels is low: from traces to 0,8%.
The higher indicators are typical of the sediments from the periphery of the
shelf and the upper part of the continental slope. The infrared spectroscopy
disclosed here the presence of aromatic structures, unlike the case with the
bitumoids.
The infrared spectra of the kerogen indicate that, as a whole, the organic
matter of the sapropels consists chiefly of aliphatic heterostructures with many
oxygen�containing groups characterizing acids and alcohols. The well expressed
peak of 1000– 1020 сm�1 is correlated to the presence of cycloparaffin structures.
What is typical here is the absence of the С=С bond of aromatic rings. Thus it
was established that the deep sea organogenic – mineral sediments from the
Fig. 6. Distribution of the main components of DSOMS, (Dimitrov, 1990), average
value (%), the symbols are the same as in fig. 3
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 15
seafloor of the Black Sea contain the main soil improvers – humus and clayey
minerals. The latter surround the mineral aggregates in the soil, stick them
together and form small aggregates that retain moist, absorb cancerogenic
elements and help plant roots reach the microorganisms, the nutrient salts
and the air.
The microelements contained in the sapropels are an object of intensive
studies using various methods: mainly atom absorption and emission spectral
analysis. It can be concluded on the basis of the high content of organic matter
in the sapropels that they have high content of Sr, U, Mo, Ti and other elements.
The concentrations of titanium are within 0,3–0,5%. There are impressively
high concentrations of molybdenum varying in different samples from 80 to
250 g/t. The distribution of the main microcomponents is shown on fig. 6 and
in table 2.
The results of the general chemical analysis of the Holocene sapropels have
considerable deviations from the indicators characterizing the common
formation models such as the Neogene clays of the Russian platform, the clays
and the claystone from the continental sector of the lithosphere, the pelagic
silicite oozes, etc. The composition of the mineral matrix of the sapropels does
not differ sharply from the composition of the pelite formations distributed on
the continents.
The comparison of the Holocene sapropels to the pelagic formations related
to the red clays and the silicite (diatomoceous) oozes shows that they occupy an
intermediate position between these two models. Depending on the content of
SiO2, Al2O3 and alkaline oxides the sapropels are close to the red clays, and
depending on the content of Fe2O3 and TiO2 – to the silicite muds.
The sapropels are a specific product of the conditions of the Black Sea.
Many authors (Lopatin, Emets 1987; Khristchev, 1987; Shimkus, Emelyanov,
Table 2. Content of microelements (g/t) in some pelite sediments (Dimitrov, Velev 1988;
Velev, Dimitrov, Feier, 1992; Shnyukov et al., 1999)
Microelements
Sapropeloids
(Black Sea)
Clay and claystone
in the lithosphere
Pelagic red
clay
Clays (West
Siberia)
V 100–120 130 120 317
Cr 40–110 100 9 160
Co 18–20 20 74 25
Ni 80–100 95 225 173
Cu 50–70 57 250 109
Ga 30 30 20 11
Sr 200–430 450 180 156
Zr 70–90 200 150 210
Mo 80–250 2 27 66
Pb 13 20 80 17
U 14 3,2 1,3 –
DIMITROV DIMITAR P.
16 ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1
1990) consider the sapropels as analogues of “oil source rocks”, while other
(Dimitrov, Velev, 1988) believe they can be used as a possible source of non�
traditional raw materials and resources.
The Djemetinian layers end the cross�section of the sediments and are
distinguished by Arhangelskiy and Strakhov (1938) as layers formed under
conditions similar to present�day conditions. The most important feature
distinguishing deep sea Djemetinian sediments is the high carbonate
coccolithophorid muds. The studies of the species composition of the
coccolithophorids (Moncheva et al., 1999) indicate that the modern sediments
and the sediments from the whole period of the Holocene are predominated by
the species Emiliania huxleyi acme, while the species Gephyrocapsa
carribianica lie at the basis of present�day layers. The lower part of the modern
sediments according to the lithological data is determined by the appearance
of the first interbeds of sapropelic sediments or the appearance of the species
Gephyrocapsa carribianika. According to the absolute datings of the lower part
of the pure Coccolith ooze, in С�544, the age is estimated at 2930 ± 110 years.
Degens, Ross (1972) point to 3090 ± 130 years – a figure close to the number
obtained by the author with regard to the lower part of unit Ia. The thickness
of the sediments on the continental slope and in the deep sea depression is
from 10–15 cm to 30–45 cm. There are only rare cases of coccolith oozes with
thickness up to 80–90 cm. Very often the coccolith oozes are interleaved by
thin (1–2 mm) strips of diatom algae. In most case the coccolith oozes are
mostly with high carbonate content decreasing due to dilution with terrigenous
material. The distribution of the modern deep sea sediments is limited by the
ratio between the biogenous and the terrigenous component affected by the
local factors of the different morpholithogenetic zones. The main charac�
teristic feature, however, remains the high biological productivity of the
coccolith phytoplankton.
The distribution by area is represented in an acceptable way by Khrischev
et al. (1988). The lithofacial map does not show the lithofacies of the diatomaceous
sediments developed in the southern part of the continental slope, at depths from
180 to about 800 m. This strip occupies an area characterized by marine complexes
of diatomea without reaching the Neoeuxinian sediments. The development of
“pure” diatomaceous sediments near the Bosphorus region may be explained by
the role of the geochemical barrier zones and the ecology of the diatom algae whose
biological productivity rises sharply here. This process benefits from the
favourable nutritional environment created by the inflow of water from the Sea
of Marmara. A field rich in diatomaceous sediments was discovered in the Danube
Canyon at depths of 250–600 m alternating with predominant amounts of
coccolith oozes. The distribution of macro� and microcomponents in the
coccolithophorid oozes is shown on fig. 1, 6. The content of Сorg. reaches 4–5%,
the amount of carbonates fluctuates from 35–40% to 90%.
The coccolith sedimentation designates a new stage in the development
of the basin under the conditions of growing eutrophication. The comparative
analysis of the coccolithophorid phytoplankton since 1965 indicates a sharp
increase in its biological productivity hence its amount in the sediments
(Sorokin, 1982).
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 17
Acknowledgements for National Science Fund and Ministry of Education
and Science: Project No 02–35, Bulgaria–Ukraine, “Non�traditional resources
from Black sea bottom and their possibilities to use as complex raw material”;
Project No 02–337, “Ancient coastlines of the Black Sea and conditions for
human presence”.
Arkhangelsky, A., N. Strakhov, 1938. Geological structure and history of development
of the Black Sea. The Academy of Sciences of the USSR Press (Moscow�Leningrad):
310. (in Russian).
Blokhina, T. 1994. Sapropel ooze of the Black Sea (compositions, genesis, utilization
prospects). Author’s PhD abstract. Kiev, National Academy оf Sciences оf Ukraine,
22. (in Russian)
Butuzova, G., Gradusov, P., Rateev, M., 1975. Clay minerals and their distribution in
the upper layers of the sediments in the Black Sea. Lithological and mineral
resources, 1, 3–11. (in Russian).
Chochov, S. D. 1984. The role of the Bulgarian Black sea shelf terrace relief on the recent
clay sedimentation. – In: Rep. 27th Intern. Geol. Congress, Moscow, v. II; 39.
Coolen, MJL; Saenz, JP; Giosan, L; Trowbridge, NY; Dimitrov, P; Dimitrov, D;
Eglinton, TI. 2009. DNA and lipid molecular stratigraphic records of haptophyte
succession in the Black Sea during the Holocene. Earth and Planetary Science
Letters. 284 (3–4): 610–621. 10.1016/j.epsl.2009.05.029
Degens, E. T. and Ross, D. A., 1972. Chronology of the Black Sea over the last 25,000
years. Chem. Geol., 10: 1–16.
Deuser, W., 1974. Evolution of anoxic conditions in Black sea during Holocene. In:
E.T. Ross (Eds.). Black Sea – Geology, Chemistry and Biology, American Association
of Petroleum Geologist Memoir, Vol. 20, Tulsa, Oklahoma, USA, 133–136.
Dimitrov, P., 1990. Geological history of the western part of the Black Sea during the
Quaternary and conditions for the formation of mineral resources. Habilitation
paper, 257 p. (in Bulgarian).
Dimitrov, P., V. Velev, 1988. On the possibilities for use of deep sea sapropelic ooze of
the Black Sea for agrobiological and industrial purposes. Oceanology, 17, S., 92–
95. (in Bulgarian).
Filipova, M., E. Bozilova, P. Dimitrov, 1983. Palinological and Stratigrafical Data about
the Quaternary from the Southern Part of the Black Sea Shelf. Oceanology, II, 24–32.
Filipova, M., E. Bozilova, P. Dimitrov, 1989. Palinological investigation of the Late
Quaternary deep�water sediments from the southwestern part of the Black Sea. Bull.
Du Musee National de Varna, 25 (40), 177–181.
Filipova�Marinova, M., 2003. Paleoenvironmental changes along Southern Black Sea
coast of Bulgaria during the last 29 000 years. Phitologia balcanica, 9 (2), Sofia,
275–293.
Georgiev, V., 1984. Accumulation of carbonates on the continental slope in the south�
west of the Black Sea during the Quarternary. – Magazine of the Bulgarian
Geological Society, 45, 2, 143–164. (in Bulgarian).
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sedimentograph (granulometer). Bulgarian Geological Association Magazine, 47,
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Magazine of the Bulgarian Academy of Sciences № 6, 30–37. (in Bulgarian)
Кhrishev Kh., V. Georgiev. 1981. Surface textures of quartz grains as a source of
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Khristchev, H. G., S. D. Chochov, V. Shopov, D. Yankova, 1988. Lithostratigraphy of
lithofacies features of the Upper Quaternary deep sea sediments of the western Black
Sea depression. Geol. Balc., 18.2, 3–17. (in Russian).
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Structure and biostratigraphic segmentation of the Quaternary sediments on the
Bulgarian shelf. Bulletin of Moscow Society of Naturalists, Geology Department,
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sea. Rev. Internationale d’Oceanographie Medicale, 101–102–103–104, 124–126.
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Quaternary period. М., Science, 239. (in Russian).
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water in the Black Sea. In the collection: Geology and mineral resources of the Black
Sea. Kiev, 412–418. (in Russian).
Shnyukov, E., S. Kleshtenko, T. Kukovskaya, 2003. Sapropel sediments of the eastern
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periphery of the Black Sea. М., Science, 210. (in Russian).
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Traverse A., 1978. Palynological Analysis of DSDP LEC 42B (1975) Cores from the
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368с. (in Russian).
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sapropeloids in the western area of the Black Sea. – Oceanology, 58–63. (in
Bulgarian).
Голоценовые осадки Черноморской впадины формировались, по нашему мнению, в
условиях геокатастрофических событий, произошедших на границе плейстоцена–го�
лоцена (8–9 тыс. лет тому назад). В результате над верхнеплейстоценовыми озер�
SAPROPELIC, DIATOMACEOUS AND COCCOLITH SEDIMENTS...
ISSN 1999�7566. Геология и полезные ископаемые Мирового океана, 2011, №1 19
ными осадками залегают органо�минеральные (сапропелевые, диатомовые и кокколи�
товые) морские осадки. Характерной чертой произошедшей катастрофы является
возникновение сероводородного заражения, которое консервировало органический ма�
териал и предохранило его от разложения. Химический состав и свойства глубоковод�
ных органо�минеральных осадков дают нам основание рекомендовать их как комплек�
сное сырье многоцелевого предназначения, и в первую очередь в области биоземледелия.
Голоценові осади Чорноморської западини, на наш погляд, формувалися в умовах
геокатастрофічних подій, які відбувалися на межі плейстоцену–голоцену (8–9 тис. р.
тому). В результаті над верхньоплейстоценовими озерними осадами залягають орга�
но�мінеральні (сапропелеві, діатомові та кокколітові) морські осади. Характерною
рисою катастрофи, що відбулася, є виникнення сірководневого зараження, що закон�
сервувало органічний матеріал і запобігло його розкладу. Хімічний склад і властивості
глибоководних органо�мінеральних осадів дають нам підставу рекомендувати їх у
якості комплексної сировини багатоцільового призначення, і в першу чергу – в біозем�
леробстві.
Received 22.09.2010
|
| id | nasplib_isofts_kiev_ua-123456789-44536 |
| institution | Digital Library of Periodicals of National Academy of Sciences of Ukraine |
| issn | 1999-7566 |
| language | English |
| last_indexed | 2025-11-30T09:12:39Z |
| publishDate | 2011 |
| publisher | Відділення морської геології та осадочного рудоутворення НАН України |
| record_format | dspace |
| spelling | Dimitrov, D. 2013-06-02T15:19:54Z 2013-06-02T15:19:54Z 2011 Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties / D. Dimitrov // Геология и полезные ископаемые Мирового океана. — 2011. — № 1. — С. 5-19. — Бібліогр.: 35 назв. — англ. 1999-7566 https://nasplib.isofts.kiev.ua/handle/123456789/44536 Holocene Black Sea basin sediments were formed in our opinion in happened geocatastrofic event on the border Pleistocene–Holocene (8–9 thousand years ago). As a result on the Upper Pleistocene lake sediments occur organogenic mineral (sapropel diatoms and coccolith) marine sediments. The characteristic features of happened catastrophe is the occurrence of hydrogen sulfide charging that conserved the organic matter and protect it from decomposition. Chemical composition and properties of deep water organogenic mineral deposits give us reason to Tip of the raw material as an integrated multi purpose and most notably in agriculture. Голоценові осади Чорноморської западини, на наш погляд, формувалися в умовах геокатастрофічних подій, які відбувалися на межі плейстоцену–голоцену (8–9 тис. р. тому). В результаті над верхньоплейстоценовими озерними осадами залягають органо-мінеральні (сапропелеві, діатомові та кокколітові) морські осади. Характерною рисою катастрофи, що відбулася, є виникнення сірководневого зараження, що законсервувало органічний матеріал і запобігло його розкладу. Хімічний склад і властивості глибоководних органо мінеральних осадів дають нам підставу рекомендувати їх у якості комплексної сировини багатоцільового призначення, і в першу чергу – в біоземлеробстві. Голоценовые осадки Черноморской впадины формировались, по нашему мнению, в условиях геокатастрофических событий, произошедших на границе плейстоцена–голоцена (8–9 тыс. лет тому назад). В результате над верхнеплейстоценовыми озерными осадками залегают органо минеральные (сапропелевые, диатомовые и кокколитовые) морские осадки. Характерной чертой произошедшей катастрофы является возникновение сероводородного заражения, которое консервировало органический материал и предохранило его от разложения. Химический состав и свойства глубоководных органо-минеральных осадков дают нам основание рекомендовать их как комплексное сырье многоцелевого предназначения, и в первую очередь в области биоземледелия. Acknowledgements for National Science Fund and Ministry of Education and Science: Project No 02–35, Bulgaria–Ukraine, “Non traditional resources from Black sea bottom and their possibilities to use as complex raw material”; Project No 02–337, “Ancient coastlines of the Black Sea and conditions for human presence”. en Відділення морської геології та осадочного рудоутворення НАН України Геология и полезные ископаемые Мирового океана Полезные ископаемые Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties Сапропелеві, діатомові і кокколітові мули (одиниці Ib, Ia) дна Чорного моря – походження, склад та властивості Сапропелевые, диатомовые и кокколитовые илы (единицы Ib, Ia) дна Черного моря – происхождение, состав и свойства Article published earlier |
| spellingShingle | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties Dimitrov, D. Полезные ископаемые |
| title | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties |
| title_alt | Сапропелеві, діатомові і кокколітові мули (одиниці Ib, Ia) дна Чорного моря – походження, склад та властивості Сапропелевые, диатомовые и кокколитовые илы (единицы Ib, Ia) дна Черного моря – происхождение, состав и свойства |
| title_full | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties |
| title_fullStr | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties |
| title_full_unstemmed | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties |
| title_short | Sapropelic, diatomaceous and coccolith sediments (units Ib, Ia) of The Black sea bottom – genesis, composition and properties |
| title_sort | sapropelic, diatomaceous and coccolith sediments (units ib, ia) of the black sea bottom – genesis, composition and properties |
| topic | Полезные ископаемые |
| topic_facet | Полезные ископаемые |
| url | https://nasplib.isofts.kiev.ua/handle/123456789/44536 |
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