New data on the history of the development of the southeastern part of the Baltic Sea from the Late Glacial to the present. Baltic Sea

1. MATERIAL AND METHOD.

2. CHARACTERISTICS OF THE BALTIC SEA AS A HABITAT.

2.1. Physical and geographical characteristics of the Baltic Sea.

1.2. Features of natural climatic conditions and hydrometeorological characteristics of the South-Eastern part of the Baltic Sea.

2.2.1. Geomorphology, relief and bottom sediments.

2.2.2. Meteorological (climatic) characteristic.

2.2.3. Hydrological characteristic.

2.3. Hydrobiological characteristics of the Baltic Sea.

2.3.1. Phytoplankton, zooplankton, zoobenthos.

2.3.2. Ichthyofauna.

3. BIOECOLOGICAL CHARACTERISTICS OF THE FISH COMPOSING THE ICHTHYOPLANKTON COMPLEX OF THE COASTAL ZONE OF THE SOUTH-EASTERN BALTICA IN 2000-2005

4. SPECIES STRUCTURE AND POPULATION OF ICHTHYOPLANKTON IN THE COASTAL ZONE OF THE SOUTH-EASTERN BALTICA.

4.1. Species composition and abundance of ichthyoplankton.

4.2. Spatial variability of species diversity and abundance of ichthyoplankton.

4.3. Seasonal variability of species diversity and abundance of ichthyoplankton.

4.4. Interannual variability of species diversity and abundance of ichthyoplankton.

5. IMPACT OF ABIOTIC FACTORS ON THE FORMATION OF THE ICHTHYOPLANKTON COMPLEX.

6. MORPHOLOGY OF FISH LARADS AND FRY AND ITS USE

FOR ENVIRONMENTAL QUALITY ASSESSMENT IN THE SOUTH-EASTERN BALTIC.

Introduction to the thesis (part of the abstract) on the topic "Ichthyoplankton of the coastal zone of the South-Eastern part of the Baltic Sea"

The study of the early ontogenesis of marine fish is associated with the development of a number of important theoretical and practical problems. The expansion of the range of the species, its adaptation to new environmental conditions is determined to a large extent by the ecological and physiological lability of the population in early ontogeny. Numerous studies testify to the decisive importance in the formation of generations of the embryonic and postembryonic periods of development.

In connection with the growing importance of marine products, problems arise not only in the development of commercial resources, but also in their protection. Successful solution of these problems requires a deep knowledge of the biology of fish in all periods of the life cycle and, above all, in early ontogenesis, which mainly determines the adaptation of the species to new environmental conditions and its survival in artificial conditions.

At present, an important place in marine ichthyology is occupied by the study of planktonic phases of fish development - pelagic eggs and larvae. Quantitative accounting of ichthyoplankton can be considered as one of the most representative methods for estimating the number of fish populations /41/.

Many species pass through two planktonic phases of life in ontogenesis (the phase of eggs and the phase of larvae); others - one planktonic phase (the larval phase). Therefore, data on the species composition and abundance of fish larvae can give good information on the species composition of the ichthyofauna. Numerous fish larvae, as consumers of plant plankton, on the one hand, and as food objects for various planktonic and nektonic organisms, on the other hand, play an important role in the tropho-dynamic processes of the sea /31/.

The history of ichthyoplankton research in the Baltic Sea is 100 years old. Their origins were German scientists from the Helgoland Biological Station and the Kiel Marine Laboratory - Ehrenbaum, Shrodtmann and Apshtein. They made the first descriptions of eggs and larvae of Baltic fish and some features of their distribution. Systematic quantitative ichthyoplankton collections in the Baltic Sea proper were started by S. Shtrodtman in 1903. GB Grauman made a significant contribution to the study of Baltic ichthyoplankton. The main direction of her research was the study of distribution features and patterns of population formation in early ontogeny (roe, larvae). The history of Soviet research was continued in Russia by the efforts of the Baltic Sea Laboratory at AtlantNIRO, restored in 1992 /128/.

The coastal zone (as a natural object) is a part of the World Ocean with an adjacent coast, formed under the influence of Holocene marine processes. It includes the coast, coast and shelf. The morphological maritime boundary of the coastal zone is an area with a sharp inflection of the transverse profile, which determines the transition of the shelf to the continental slope. The land boundary of the coastal zone is limited by the position of morphological or lithological features of the marine impact of the Holocene time (the first terrace or marine deposits not covered by aerial deposits) /1/.

The shallow coastal zone of the South-East Baltic is an area that provides the formation of stocks of commercial species and small non-commercial fish, which play an important role in the trophic chains of the ecosystem. Small groups of herring and sprats spawn here - one of the main commercial objects of the Baltic Sea. At the end of summer - beginning of autumn, coastal shallow water becomes a feeding area for juvenile sprat. At the same time, the coastal zone is the focus of many interests, which are often incompatible with the goals of environmental conservation and sustainable fisheries. Thus, the coastal area of ​​the South-Eastern Baltic (Kaliningrad region) has become an arena of intensive management, which is developing rapidly due to the activation and development of investment-attractive sectors of the economy associated with the use of coastal zone resources (for example, the development of oil fields). In addition, the study area is the final water body for the bulk of both pollutants and natural substances /1/. The main way to preserve the ecosystem in the conditions of anthropogenic pressure is to monitor the state of natural ecosystems, an element of which is the ichthyoplankton complex, which is formed in coastal zone. In addition, the study of the dynamics of ichthyoplankton makes it possible to assess the effectiveness of the natural reproduction of fish stocks and establish the limits of safe fishing.

Studies of the early ontogenesis of fish, conducted by AtlantNIRO in 2000-2005, were carried out with the aim of understanding the mechanism of population formation, assessing changes in the qualitative and quantitative composition of ichthyoplankton, which can serve as an important indicator of future changes in the adult community. However, despite the century-old history of studying the ichthyoplankton of the Baltic Sea, the composition and its spatial and temporal dynamics in the coastal zone of the South-East Baltic of the Kaliningrad region still remain poorly understood. In this paper, for the first time, the results of long-term ichthyoplankton studies in the coastal region are summarized and analyzed. Purpose and tasks of the work.

The aim of the work is: to study the structure and patterns of formation of the ichthyoilactic community of the coastal zone of the South-East Baltic under the influence of abiotic factors.

In the process of work, the following tasks were solved:

1) Assess the species structure and abundance of ichthyoplankton in the coastal zone of the South-Eastern Baltic Sea;

2) Analyze spatial, interannual and seasonal changes abundance and distribution of fish eggs and larvae;

3) Compile a catalog of fish larvae and fry found in ichthyoplankton in 2000-2005;

4) To analyze the influence of abiotic factors on the distribution and abundance of ichthyoplankton;

5) Study the morphology and identify the presence or absence of morphological abnormalities in the development of fish larvae and fry.

Scientific novelty. On the basis of modern data on the ichthyoplankton of the coastal zone of the South-East Baltic, the species structure and population dynamics of the ichthyoilactic complex, as well as species diversity using information indicators, were studied for the first time. For the first time, a catalog of larvae and fry of fish found in the ichthyoplankton of the South-Eastern Baltic has been compiled. The abiotic factors influencing the formation of the ichthyoplankton community have been identified. For the first time, studies of the morphological state of larvae and fry of fish in the study area were carried out in order to identify deformities in development and slowly accumulating changes in the rate of differentiation and the rate of their growth.

Practical significance of research. The results of the work serve as initial information on the state of stocks and habitats of the Baltic fish in accordance with the thematic plan of research work of the Federal State Unitary Enterprise AtlantNIRO. The data are presented at the ICES scientific session to develop ecosystem assessments of the state of stocks and recommendations for fishery management measures, and are also used to monitor the areas of soil dumps and infrastructure of the Kravtsovskoye (D-6) oil field in the Baltic Sea. The performed researches allow to plan accounting surveys for ichthyoplankton. The compiled catalog of fish larvae and fry gives an idea of ​​the ichthyoplankton community of the study area. Studies on the assessment of the morphological state of fish larvae and fry revealed the absence of anomalies in their development at early ontogenetic stages.

Provisions for defense:

1) Features of the species structure of the ichthyoplankton community of the coastal zone of the South-East Baltic of the Kaliningrad region and its spatial and temporal variability;

2) The nature of the relationship between the variability of species composition, the number of ichthyoplankton and hydrological factors;

3) Evaluation of the possibility of using morphological analysis of fish larvae and fry to characterize the quality of the environment in the South-East Baltic.

Approbation of work. The results of scientific research underlying the dissertation were repeatedly presented at seminars of the Department of the Baltic Sea and Limans, at a meeting of the biological section of the Scientific Council of AtlantNIRO (2005), at a scientific session of ICES (Copenhagen, Denmark, 2002), at the Second All-Russian School of Marine biology in the section "Marine flora and fauna of the northern latitudes: mechanisms of adaptation and regulation of the growth of organisms" (Murmansk, 2003), at the International Scientific Conference "Innovations in Science and Education - 2005", dedicated to the 75th anniversary of the founding of KSTU and the 750th anniversary Koenigsberg-Kaliningrad (Kaliningrad, 2005).

The author expresses his sincere gratitude to the supervisor of the dissertation work, Doctor of Biological Sciences, Professor Shibaev Sergey Vadimovich. I express my deep gratitude to Cand. biol. Sciences, senior researcher Karaseva Elena Mikhailovna and Senior Researcher laboratory of the Baltic Sea, the head of the ecology group Alexander Stepanovich Zezere for comprehensive assistance and critical remarks on the essence of the work.

I consider it necessary to thank the head of the Department of the Baltic Sea and Limans of AtlantNIRO, Ph.D. biol. Sciences. Feldman Valery Nikolaevich, Head of the Baltic Sea Laboratory Nikolai Alexandrovich Nazarov, researcher of the Baltic Sea Laboratory Tatyana Georgievna Vasiliev for constant attention and support in the work. I would like to express my gratitude to the employee of the Baltic Sea Laboratory V.P. Shopov for direct participation in the collection of materials for writing a dissertation.

1. MATERIAL AND METHOD

The work used materials obtained during ichthyoplankton surveys in the coastal zone of the South-Eastern Baltic Sea within depths from 5 to 50 m (subarea 26, EEZ Russian Federation, Kaliningrad region), in research expeditions on the ships STM-K-1711 "Atlantniro", STM-K-1704 "Atlantis", SChS-7011 "Baltika" and MRTK "Udria" for the period 2000-2005. (May-June, July, August, October). The layout of ichthyoplankton stations is shown in Figure 1.

In scientific expeditions, when collecting ichthyoplankton, the IKS-80 ichthyoplankton net was used: a standard (or half a meter, respectively, throat area) net with a throat area of ​​0.5 m2 and a total length of 5 m. The inner diameter of the hoop is 80 cm. This net is a conical bag from a silk sieve (gas No. 21) and calico, the base of which is reinforced with a metal hoop, and the top ends with a glass. The length of the mesh cone from the top to the base along the side is 300 cm, the circumference of the base is 252 cm, the circumference of the top is 25 cm.

Samples were collected by means of vertical (total) catches (the entire study period is an indicator of the number of specimens/m2), as well as surface or horizontal catches (July is an indicator of the number of specimens/catch).

Vertical fishing was carried out with an ichthyoplankton net from the bottom to the surface, regardless of the depth of the place, with additional work by the ship's engine during the station. The net, attached to the torso of the winch and equipped with a load, is carried overboard and lowered down until the net hoop reaches the surface of the water. Then the counter is set to zero and with the help of a winch the net is lowered to a predetermined depth, noting the angle of deviation of the cable from the vertical. Having stopped the network, they immediately begin to select it at a speed of 1m / s. When making a total catch, they stop the net, usually not reaching the bottom of about 5 m.

Surface fishing was carried out on the circulation of the vessel for 5 minutes (net depth from 1.5 to 3.0 m).

After rising to the deck, the nets were rinsed in buckets, and then the catch of the IKS-80 net was filtered through a sieve No. , run time) and filled with 4% formalin solution (9 volumes of water and 1 volume of 40% formalin).

Figure 1 - Scheme of the location of ichthyoplankton stations in the coastal zone of the South-Eastern Baltic (26th subarea, EEZ of the Russian Federation, Kaliningrad region) in 2000-2005.

Data for each sample, indicating: number, coordinates, date, time of fishing, depth of place, weather conditions, length of the etched cable, angle of deviation of the cable, were recorded in the plankton log. The samples were delivered to the shore for office processing. Processing of ichthyoplankton samples was carried out according to the standard method: identification of eggs and larvae of fish, accounting for their abundance and measurement of the length of larvae, which was carried out using the eyepiece-micrometer of the MBS-9 binocular. The measurement accuracy was 0.1 mm /42, 85/.

Between 2000 and 2005 19 surveys and 457 ichthyoplankton stations were made, 764 specimens were identified and measured. eggs and 14135 specimens. fish larvae (table 1 and 2).

Table 1 - Number of ichthyoplankton stations carried out in the coastal zone of the South-East Baltic Sea in 2000-2005

Years Months May-June July August October

2000 5 (24-27.05) 74 (04-06.07) - -

2001 8 (23-28.05) 88 (04-06.07) 8 (22-23.08) 8 (24-25.10)

2002 11 (20.05-01.06) 92 (08-11.07) 14 (24-27.08) -

2003 20 (21.05-06.06) - 16 (26-31.08) 4 (31.10-01.11)

2004 10 (20.05-03.06) 30 (28-29.07) 16 (12-15.08) 9 (28-31.10)

2005 18 (22.05-02.06) - 17 (03-07.08) 9 (09-11.10)

TOTAL 72 284 71 30

Table 2 - Volume of collected and processed material

Completed ichthyoplankton surveys 19

Collected ichthyoplankton samples 536 including:

Vertical fishing 394

Horizontal fishing 142

Measured and identified by species of eggs and larvae of fish, ind. 14899 including:

Caviar, specimen 764

Larvae, specimen: 14135

Including larvae for morphometric analysis, ind. 698

In the areas of accumulation of fish larvae, an additional collection of ichthyoplankton was carried out in order to identify and study morphological deviations in the development of fish larvae and fry. During the voyage of STM K-1711 "Atlantniro" to the Baltic Sea, ichthyoplankton samples were collected. From May 15 to June 2004, and also from May 22 to June 01, 2005, 27 ichthyoplankton samples were collected in the areas of accumulation of fish larvae by vertical fishing of the bottom-surface layer. The IKS-80 net served as a fishing tool. In the period from August 07 to 26, 2004 and from August 2 to August 17, 2005, larvae and fry of fish caught on ichthyoplankton (IKS-80) and mysid surveys (Isaacs-Kidda trawl) were studied. 79 samples were collected, 698 specimens were measured. fish larvae and fry (Figure 2-3, Tables 2 and 3).

Monitoring of the morphological state of fish larvae included: 1) visual testing of fish larvae from the monitoring area; 2) measurement of various morphometric parameters of the body in order to identify slowly accumulating changes in the rate of differentiation and growth rate of fish larvae and assess the degree of interannual differences.

Visual testing of larvae, larvae-fry and fry of fish included the detection of the following anomalies /142/: 1) absence of the lower jaw, curvature of the jaws; 2) defects in the development of the eyes (absence or deformation of the lens, absence or mosaic color of the iris); 3) defects in the development of the digestive system (abnormally shortened or thickened intestinal tube); 4) abnormal type of pigmentation; 5) fused individuals.

The measurement of various morphometric parameters of the body was carried out according to the following scheme:

Sprat (mm): 1. Total length (to the end of the fin fold or tail rays); 2. Standard length (to the end of the chord); 3. Preanal distance (from the tip of the upper jaw to the anus); 4. Postanal distance (from the anus to the end of the tail); 5. Head length (from the end of the upper jaw to the base of the pectoral fin); 6. Head height; 7. Body height in the region of the dorsal fin anlage; 8. Measurement of the length and height of the yolk sac (if any).

Steers (mm): 1. Overall length; 2. Preanal distance; 3. Postal distance; 4. Head length; 5. Predorsal length (from the end of the upper jaw to the end of the dorsal fin); 6. Length of the caudal peduncle (from the end of the dorsal fin to the beginning of the caudal fin).

The work was carried out in two stages:

1). Ichthyoplankton survey (May and August): For this station, a double fishery with an ichthyoplankton net was carried out. The first sample was fixed with formalin.

The second was immediately sorted to obtain fish larvae, which were measured according to the above scheme. The analysis presented all available size classes at 0.5 mm intervals. In samples in each size class, at least 5, and in modal classes, at least 10 larvae and fry of each species were measured with an accuracy of 0.1 mm;

Figure 2 - Scheme of stations for morphological monitoring of fish larvae in May and August 2004-2005. (fishing gear - ichthyoplankton net IKS-80) in August 2004-2005. (fishing gear - trawl Isaacs-Kidda)

Table 3 - Number of stations completed for morphological monitoring of fish larvae in 2004-2005

YEAR Date Fishing gear Number of stations Industrial fish larvae ereno 4 malys sprat gobies

2004 15.05-06.06 IKS-80 10 190 -

11-23.08 IKS-80 11 - 21

17-20.08 Isaacs-Kidda trawl 9 78 109

TOTAL 30 268 130

2005 22.05-01.06 IKS-80 17 125 -

02-12.08 IKS-80 18 - 27

08-17.08 Isaacs-Kidda trawl 14 64 84

TOTAL 49 189 sh

2). Selection of fish larvae and fry during mysid survey. The survey is carried out with a 10-foot model of the Isaacs-Kydd trawl with an ichthyoplankton net insert (gas #21). Trawl stations are operated only during the hours of darkness (approximately from midnight local time until dawn).

The trawl is operated from the port (or starboard) side of the vessel. The technique of releasing and receiving a trawl on board in the conditions of an STM-type vessel is being worked out in the course of experimental work, taking into account the technical capabilities of the vessel. Standard trawls are carried out by step fishing from the bottom to the surface.

The order of execution of trawling. Upon reaching the trawling point, the navigator slows down the speed of the vessel to 3 knots, switches on the echo sounder in the mode of operation with IGEK and releases the IGEK. After that, he gives a command to the deck to start setting the trawl. On this command, the employee, who is at the side, throws the net part of the trawl overboard and gives the command to the navigator to poison the winch warp. The pickling of the warp is first carried out at the first speed, after immersing it in water - at the second speed. At the same time, it is constantly monitored so that slack and warp sag do not form during pickling. this may cause the trawl to roll over.

When setting the trawl, the navigator monitors the trawl's immersion using the echo sounder and IGEK readings. After the trawl enters the near-bottom horizon and the pickling of the warp stops, the time is recorded (by a stopwatch), because from this moment the trawl starts to catch. Further, “stepped” fishing along the horizons is carried out. The distance between the horizons is kept the same, the optimal distance is 10 m, but depending on the specific conditions, it can be somewhat less (7-8 m) or more (10-12 m).

As the practice of surveying with the Isaacs-Kydd trawl in the Baltic Sea has shown, the optimal trawl time on each horizon is 1 minute. The transition from one horizon to another should be carried out smoothly, without jumps. On the echo tape, the trawl line should look almost like an oblique line. To do this, the trawl is lifted to the next horizon at the first speed. The last horizon is the surface layer. The exit of the trawl to the surface is monitored by an employee on deck. He instructs the navigator to stop the winch and marks the time. After the time of trawling in the surface horizon, the employee instructs the navigator to select the trawl and slow down to the smallest speed.

The time of work with the trawl is recorded using a stopwatch. The stopwatch is switched on after the trawl has reached the bottom horizon and the winch has stopped. When the trawl moves from one horizon to another, the stopwatch continues to run. The stopwatch is turned off after the surface horizon has been completed, the hauling of the trawl has begun and the speed has slowed down.

The trawling course is selected depending on the weather conditions. In calm weather (wind up to 3 points) it is advisable to trawl along the isobath or downwind. In fresh weather (wind force more than 3 points), the optimal trawling course is with the wind blowing against the vessel's cheekbone.

Catch processing. After the lifting of the trawl is completed, with the help of a special exhaust end, the end of the trawl is pulled on board, then the entire net part. After that, it is fixed on the duck, and the buffoon is suspended vertically and washed off with water from a hose so that all the animals stuck to the sieve are washed into the glass. Next, the contents of the glass are poured into a bucket. Fish larvae and fry were taken from 1/10 of the mysid net catch before formalin fixation and were examined immediately. The obtained number of larvae and fry of fish from 1/10 of the part was recalculated for the entire volume of the sample.

Filling out the journal and labels. The survey log contains all the necessary information that will be required for further processing and analysis of the collected material. The journal is filled after each station. The following data is entered into the journal: 1) station number (continuous numbering); 2) Station coordinates; 3) Completion date; 4) Station start and end time; 5) Depth of the station site; 6) The length of the etched winch warp; 7) The speed of the vessel during the execution of the station (in knots); 8) Fished horizons; 9) Trawling time on the horizon; 10) The total duration of trawling (from reaching the near-bottom horizon to the end of fishing on the surface horizon in minutes and seconds, by stopwatch); 11) The mass of the caught jellyfish; 12) What part of the sample is fixed (to be filled in in case of taking a sub-sample); 13) Water temperature and salinity along the horizons from the bottom to the surface /67, 73, 76/.

The label indicates the minimum data that makes it easy to determine which station a given sample belongs to, even if part of the record is erased.

The following data must be indicated on the label: 1) Date of completion of the station; 2) station number; 3) Depth of place; 4) The total duration of the trawl. The standard label (parchment) is filled in with a pencil.

The total amount of collected and processed material in 2000-2005. presented in table 3

Ichthyoplankton samples were collected at the sites of hydrological stations.

Hydrological observations in the coastal zone of the South-East Baltic in 2000-2005. were carried out by the SBE-19 probe (Sea Bird Electronic, Ltd., USA), which was attached to the frame of the FSI oceanological complex, by continuous sounding of the bottom-surface layer. Temperature, salinity and concentration of oxygen dissolved in water were measured at each station. The oxygen sensor was calibrated at four deep water stations in the central part of the Gdansk Basin. Water samples were taken using the rosette of the FSI complex. The concentration of oxygen dissolved in water was determined by the Winkler method on a Dosimat 715 titration stand (Hydrobios, Germany) /62-77/.

To study the species diversity of the ichthyoplankton complex of the coastal zone of the ichthyoplankton complex, the following indices and indicators were used /2, 60,102/:

Shannon species diversity index Н= - (1) y^(^-l)

Simpson species diversity index D= 1- A d^dg ^ (2)

Dominance index (according to Simpson, 1949) С= 2J 77 (3)

1 \ N) where ni is the abundance of each species; N is the total number of ichthyoplankton. H

Pielow's evenness index E= ,

4) where H is the Shannon species diversity index; n is the number of ichthyoplankton species.

For a comparative assessment of the qualitative composition of ichthyoplankton complexes of vertical and horizontal catches, the coefficient of species similarity (S) was used, to take into account quantitative characteristics - the index of species similarity of A. S. Konstantinov (K):

2C where A is the number of species in sample A; B is the number of species in sample B; C is the number of species common to both samples.

K=^mm(pAj,pB), (6) where paj and pb,i are the proportion of the i-th element in systems A and B, respectively; n is the number of elements that are the same for both systems. O

During the mysid survey, the number of larvae (N) was calculated in ind./1000 m: P

Number of larvae N=-^-1000) (7) o where nj - number of fish larvae in the catch, ind.; 1000 - conversion factor per 1000 m; V is the volume of filtered water, m3.

The volume of filtered water V = svl, (8) L where s is the area of ​​the trawl mouth, 7 m; v - trawling speed (3 knots or 1.54 m/s); t - duration of trawling, sec.

In the morphological analysis of fish larvae, the following statistical indicators were used /85/: "V 2 X Xi

Standard deviation d = \) , (9) n where Xj - value of options; x - arithmetic mean; n is the number of options.

Standard error. r ~ /n "^^ where d2 is the standard deviation; n is the number of options.

Fisher criterion F = , (11)

O 2 where - Z21 and S22 - standard deviations of two sets of data.

Normalized deviation t \u003d g, (12) where - x 1 and x2 - arithmetic mean; 2 are the standard errors of the two datasets.

The calculation of statistical parameters and the construction of statistical graphs were carried out using the program STATISTICA v 6.0 /86/.

Dissertation conclusion on the topic "Ichthyology", Ivanovich, Victoria Mikhailovna

1. In the composition of the coastal ichthyoplankton of the South-East Baltic, 4 species of eggs and 15 species of fish larvae and fry were found. They can be attributed to two main assemblages: 1) pelagic eggs and larvae of species that breed mainly in the water column of deep-water basins and coastal zone (sprat prevailed); 2) the dominant group - larvae of species with bottom eggs, breeding in the shallow coastal zone (small goby predominated).

2. The ichthyoplankton community of the coastal zone of the South-Eastern Baltic belongs to the group with medium and low biotic diversity. The number of species is distributed unevenly, and the dominant role in the ichthyoplankton community is played by a limited number of species, which is a characteristic feature of the study area.

3. Seasonal variability of ichthyoplankton in the coastal zone of the South-East Baltic is pronounced. Peak numbers and maximum amount species recorded in July. The longest period of occurrence in ichthyoplankton is in eggs (May-July) and larvae of sprat (May-August), as well as in larvae of the small goby (May-October).

4. Interannual variability in the abundance and species composition of ichthyoplankton in the coastal zone of the South-East Baltic was revealed. The largest abundance and species richness of eggs were observed in 2001. The peak of abundance and species richness of fish larvae was recorded in 2000.

5. The most noticeable influence on the formation of the abundance and species composition of ichthyoplankton in the coastal zone of the Baltic Sea in 2000-2005. provided the temperature regime of the waters. Interannual and seasonal fluctuations in the abundance and spatial distribution of ichthyoplankton were due to temperature characteristic seasons (warm or relatively cold).

6. In the area of ​​the Vistula Spit, in contrast to the rest of the study area, the relationship with elevated temperatures and the concentration of fish eggs and larvae was insignificant. This area is characterized by a great influence on the distribution and abundance of ichthyoplankton of the processes of interaction with the deep-water part of the Gulf of Gdansk. Therefore, here the maximum species diversity and abundance were determined to a greater extent by the removal of ichthyoplankton (sprat, sea burbot, etc.) from the seaward part.

7. The variability of the species composition and abundance of ichthyoplankton is of a natural nature, associated with more or less favorable hydrological conditions for reproduction and is within the limits of natural fluctuations.

8. Morphological analysis of the state of larvae, fry of sprat and small goby showed the absence of deviations and anomalies in their development. The morphometric characteristics of the ichthyoplankton of these fish species corresponded to the values ​​obtained in studies more than 40 years ago and taken as the “norm”. The process of formation of morphological deviations of fish larvae and fry is not yet affected by anthropogenic factors. To assess the quality of the environment in the South-East Baltic, the morphological analysis of larvae and fry must be considered in the long term at the genetic level.

List of references for dissertation research candidate of biological sciences Ivanovich, Victoria Mikhailovna, 2006

1. Aibulatov, N.A. Activity of Russia in the coastal zone of the sea and problems of ecology / N.A. Aibulatov; under. ed. IN AND. Osipov, Russian Academy of Sciences, Inst. of Oceanology. P.P. Shirshov. -M, 2005. - 364 p.

2. Alimov, A.F. Diversity in animal communities / A.F. Alimov // Biol. diversity approaches to study and conservation: Mater, Conf. Biol. in-ta RAS and Zool. Institute of RAS, Leningrad, February 14-15. and May 14-15, 1990 - St. Petersburg, 1992. - S. 153162.

3. Alisov, B.P. Climatology course / B.P. Alisov. L .: Gidrometeoizdat, 1952. - Part 1, Part 2. - 487 p.

4. Antonov, A.E. Large-scale variability of the hydrometeorological regime of the Baltic Sea and its impact on the fishery / A.E. Antonov L.: Gidrometeoizdat, 1987.-248 p.

5. Anthropogenic impacts on coastal marine ecosystems: collection of scientific articles. M.: ed. VNIRO, 1986.-182 p.

6. Appolov, A.B. Some results of studies of macrobenthic fauna in the Eastern Baltic in 1986-1988. / A.B. Appolov // Actual problems of fishery science in the work of young scientists: Sat. scientific tr. / VNIRO. M.: Ed. VNIRO, 1990.-S. 40-58.

7. Arsen'eva, N.Ya. Calculation of atmospheric precipitation and evaporation in the Baltic Sea for 1951-1970. / N.Ya. Arseniev // Tr. GOIN. 1978. - Issue. 147. -S. 82-102.

8. Atlas of waves and winds of the Baltic Sea. Tallinn, 1965. - 87 p.

9. Atlas of waves and winds of the Gulf of Finland. L.: Gidrometeoizdat, 1967. - 48 p.

10. Atlas of hydrometeorological phenomena dangerous and especially dangerous for navigation and fishing. North and Baltic seas. L., 1980. - 168 p.

11. Atlas of typical wind fields. Klaipeda, 1980. - 180 p.

12. Babich, S.V. Probabilistic analysis and modeling of synoptic, seasonal and interannual variability of wind and waves / S.V. Babich // Probabilistic analysis and modeling of oceanological processes. L .: Gidrometeoizdat, 1984.- S. 43-78.

13. Betin, V.V. Ice conditions in the area of ​​the Baltic Sea and on the approaches to it and their long-term changes / V.V. Betin // Tr. GOIN. 1957. - Issue. 41. - S. 54-125.

14. Betin, V.V. Permanent Currents in the Open Part of the Baltic Sea Proper /

15. B.V. Betin, P.V. Panteleev // Collection of works of the Leningrad GMO. 1968. - Issue. 5.1. C.55-95.

16. Betin, V.V. Seasonal variations of the scheme of constant currents in the Baltic Sea and their changes under the influence of the wind / V.V. Betin, P.V. Panteleev // Collection of Leningrad GMO and Petrozavodsk GMO. 1970. - Issue. 6. - S. 45-69.

17. Biryukov, N.P. Baltic sprat (Biological state and economic use) / N.P. Biryukov. L .: Publishing house Leningrad. un-ta, 1980. - 144 p.

18. Borisenko, M.M. Some results of studies of the regime of strong winds in the Baltic and in the north-west of the ET USSR / M.M. Borisenko, N.K. Kravchenko // Tr. Zap.-Sib.NIGMI. 1979.-№45.-S. 41-51.

19. Borisov, A.A. Climatic features of the Kaliningrad region / A.A. Borisov // Izv.VGO. 1972. - No. 2. - S. 84-91.

20. Buz, A.I. Conditions for the formation of squalls in the south of the Baltic states / A.I. Buz //Tr.GMTs. -1973.-Iss. 105.-S. 46-54.

21. Buz A.I. Questions of forecasting wind speed / A.I. Buz // Weather-forming processes and dangerous weather phenomena over Lithuania and the Kaliningrad region. L .: Gidrometeoizdat, 1988. - S. 120-128.

22. Wind and waves in the oceans and seas. Reference data. Register of the USSR. L.: Transport, 1974. - 360 p.

23. Hydrometeorological characteristics of the Baltic Sea / comp. L.F. Rudovica. -M.: Gidrometeoizdat, 1943. 249 p.

24. Hydrometeorological conditions of the shelf zone of the seas of the USSR. Handbook.T. 1. -Issue 1. L.: Gidrometeoizdat, 1983. - 173 p.

25. Hydrometeorology and hydrochemistry of the seas. T.Z. Baltic Sea. Issue. 2. Hydrometeorological conditions and oceanological foundations of the formation of biological productivity / ed. F. S. Terzieva /and others/ St. Petersburg, Gidrometeoizdat, 1994.-435 p.

26. Hydrometeorology and Hydrochemistry of the Seas of the USSR. T.Z. Baltic Sea. Issue. 1. Hydrometeorological conditions / ed. F. S. Terzieva /and others/ St. Petersburg, Gidrometeoizdat, 1992.-450 p.

27. Grauman, G.B. Spawning ecology of the Baltic cod (Gadus morhua callarias L.) and factors that determine its effectiveness / G.B. Grauman. Kaliningrad, 1968. -20 p.

28. Davidan, I.N. Wind waves in the World Ocean / I.N. Davidan, L.I. Lopatukhin, V.A. Rozhkov. L.: Gidrometeoizdat, 1985. - 256 p.

29. Davidan, I.N. Long-term changes in hydrological conditions in the central part of the Baltic Sea and their connection with atmospheric processes / I.N. Davidan, A.E. Mikhailov, A.I. Smirnova // Meteorology and hydrology. 1989. - No. 8. - S. 6573.

30. Dekhnik, T.V. Ichthyoplankton of the Black Sea / T.V. Dekhnik. Kyiv: "scientific thought", 1973.-235 p.

31. Materials of the Second All-Russian School of Marine Biology, Murmansk, November 3-5, 2003. Apatity: Ed. Kola scientific center RAN, 2004. - S. 178181.

32. Ivanovich, V.M. Ichthyoplankton research in the coastal zone of the South-Eastern Baltic / V.M. Ivanovich // Fisheries. 2006. - No. 5. - S. 76.

33. Ignatavichene, I.O. On some features of fluctuations in the circulation of the atmosphere and the climate of the Baltic states / I.O. Ignatavichene // Articles on hydrometeorology. -Vilnius, 1971.-S. 61-72.

34. Research on the dynamics of the waters of the Baltic Sea / ed. R.V. Ozmidova M.: ed. IOAN, 1977.-306 p.

35. Ichthyoplankton and its importance for the knowledge of the ichthyofauna of the World Ocean / Proceedings of the Institute of Oceanology. P. P. Shirshova / M .: Nauka, 1986, - T. 116. 176 p.

36. Casanova, I.I. Key to eggs and larvae of fish of the Baltic Sea and its bays / I.I. Casanova, under ed. ON THE. Dmitrieva // Biology and fishing of the main commercial fish of the Baltic Sea. T. XXVI.: tr. VNIRO. 1954. - S. 221-265.

37. Kaleis, M.V. Modern hydrological conditions in the Baltic Sea / M.V. Kleis //Ambio Special Report. 1976. - No. 4. - P. 37-44.

38. Kalinina, E.M. Reproduction and development of the Azov-Black Sea gobies / E.M. Kalinin. Kyiv: Nauk, Dumka, 1976. - 118 p.

39. Kaushila, K.I. Experience of regionalization of the Southern Baltic according to local factors of climate formation / K.I. Kaushila // Articles on hydrometeorology. Vilnius, 1970.- S. 52-62.

40. Krylova, V.D. Disturbances in the development of Bester at the early stages of ontogenesis with artificial breeding / V.D. Krylov // Proceedings. report V All-Union Conference on the early ontogenesis of fish, Astrakhan, 1-3 Oct. 1991 M., 1991. - S. 194-198.

41. Lebedeva, O.A. Influence of anthropogenic factors on the early ontogenesis of fish / O.A. Lebedev // Proceedings. report V All-Union Conference on the early ontogenesis of fish, Astrakhan, 1-3 Oct. 1991-M., 1991.-S. 149-151.

42. Mykolayunas, M.M. Spatial-temporal structure of dangerous winds over the water area of ​​the transition from the ports of the southern Baltic to Atlantic Ocean/ MM. Mykolayunas: Information letter of the Lithuanian UGKS. Vilnius, 1987. - 124 p.

43. Mikhailov Yu.D. Probabilistic characteristics of coastal currents of the Baltic Sea / Yu.D. Mikhailov // Tr. GOIN. 1972. - Issue. 111. - S. 76-97.

44. Monin, A.S. Variability of the World Ocean / A.S. Monin, V.M. Kamenkovich, V.G. Court. L.: Gidrometeoizdat, 1974. - 262 p.

45. Moskalkova, K.I. Morpho-ecological features of the development of the round goby Neogobius melanostomus (Pall.) / K.I. Moskalkova // Morpho-ecological analysis of fish development. M.: Nauka, 1967. - S. 48-76.

46. ​​Nemova, N.N. Biochemical indication of the state of fish / N.N. Nemova, R.U. Vysotskaya; ed. M.I. Shatunovsky; IT Biology KarRC RAS. M.: Nauka, 2004.-215 p.

47. Nikolsky, G.V. Private ichthyology / G.V. Nikolsky. Ed. 3rd, rev. and additional Textbook for universities in the specialty "Ichthyology". M.: "High School", 1971. -472 p.

48. Odum, Yu. Fundamentals of ecology / Yu. Odum. M.: Mir, 1975. - 740 p.

49. Report on the flight SRT-4379 to the South-East Baltic in the area of ​​the Gdansk Bay and in the Latvian zone to the Shventoy point in September 1972 / Isp. N.N. Yanchenko and others, Kaliningrad, 1972.-20 p.

50. Report on the implementation of expeditionary oceanological work on the R/V Monocrystal to study drift and non-periodic currents in the water area adjacent to the D-6 structure. Kaliningrad, 1994. - 22 p.

51. Research report on the 25th voyage of R/V-8390 "Atlantis" to the Baltic Sea in May-June 2000 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2000. 43 p.

52. Report on ichthyoplankton and hydrological survey in the area of ​​the coast of the Kaliningrad region on SChS-7011 "Baltic" in the Baltic Sea in July 2000 / Isp. E. A. Gribov et al., Kaliningrad, 2000. 20 p.

53. Research report on the 30th voyage of STM-8391 "Atlantniro" to the Baltic Sea in May 2001 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2001. -42 p.

54. Report on ichthyoplankton and hydrological survey in the area of ​​the coast of the Kaliningrad region on SChS-7011 "Baltic" in the Baltic Sea in July 2001 / Isp. E. A. Gribov et al., Kaliningrad, 2001. 18 p.

55. Report on research work MRTK-0749 "Udria" in the Baltic Sea in August 2001 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2001. 13 p.

56. Research report on the 30th voyage of R/V-8390 "Atlantida" to the Baltic Sea in October 2001 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2001.-43 p.

57. Research report on the 33rd voyage of STM-8391 "Atlantniro" to the Baltic Sea in May-June 2002 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2002. 44 p.

58. Report on ichthyoplankton and hydrological survey in the area of ​​the coast of the Kaliningrad region on SChS-7011 "Baltic" in the Baltic Sea in July 2002 / Isp. E. A. Gribov et al., Kaliningrad, 2002. 21 p.

59. Report on research work MRTK-0749 "Udria" in the Baltic Sea in August-September 2002 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2002, -11 p.

60. Research report on the 37th voyage of STM-K-1711 "Atlantniro" to the Baltic Sea in May-June 2003 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2003. 43 p.

61. Report on research work MRTK-0749 "Udria" in the Baltic Sea in August-September 2003 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2003. -19 p.

62. Research report on the 34th voyage of the STM-K-1704 "Atlantis" to the Baltic Sea in October-November 2003 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2003. 47 p.

63. Research report on the 40th voyage of STM-K-1711 "Atlantniro" to the Baltic Sea in May-June 2004 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2004. 48 p.

64. Research report on 41 voyages of STM-K-1711 "Atlantniro" to the Baltic Sea in August 2004 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2004. 29 p.

65. Research report on the 42nd voyage of STM-K-1711 "Atlantniro" to the Baltic Sea in October-November 2004 / Beginning. expeditions of A. S. Zezer, Kaliningrad, 2004. 54 p.

66. Essays on the biological productivity of the Baltic Sea / Under. ed. D. E. Gershanovich. M., 1984.- 389 p.

67. Patokina, F.A. Ecology of nutrition and nutritional relations of mass fish of the Baltic Sea / F.A. Patokina // Fishing Issues. 2000. - V. 1, No. 2-3, part II. - S. 86-87.

68. Pinchuk, V.I. On the species composition of goby fish of the genus Pomatoschistus (Gobiidae) in the seas of the USSR / V.I. Pinchuk, M.Ya. Savchuk // Questions of ichthyology. 1982. - Vol. 22, issue. 1,-C. 9-14.

69. Pomeranets, K.S. Spatial variability of water temperature in the Baltic Sea / K.S. Pomeranian // Tr. GOIN. 1972. - Issue. 110. - S. 37-44.

70. Preliminary assessment of the current state of biodiversity within the Kaliningrad region (final): research report // Book 1. X. D. No. 9 / E / Supervisor M. M. Khlopnikov. Kaliningrad. 1996. - 326 p.

71. Problems of research and mathematical modeling of the Baltic Sea ecosystem. International project "Baltic". Issue 1.-L.: Gidrometeoizdat, 1983.-255 p.

72. Russ, T.S. Guidelines for the collection of eggs, larvae and fry of fish / T.S. Russ, I.I. Casanova; M: Food industry., 1966. 42 p.

73. Rokitsky, P.F. Biological statistics / P.F. Rokitsky. 3rd ed., rev. Minsk: Higher. school, 1973. - 320 p.

74. Guidelines for the calculation of the elements of the hydrological regime in the coastal zone of the sea and in the mouths of rivers during engineering surveys. Moscow: Gidrometeoizdat, 1973. 112 p.

75. Soskin, I.M. Currents of the Baltic Sea based on the processing of hydrological observations by the dynamic method / I.M. Soskin, L.N. Kuznetsova, V.I. Solovyov // Tr. GOIN 1963. - Issue. 73 - S.76-95.

76. Soskin, I.M. International expeditionary research on the Baltic Sea / I.M. Soskin // Information collection. No. 4 - L .: Gidrometeoizdat, 1957. S. 8891.

77. Soskin, I.M. Empirical dependencies for calculating wind currents / I.M. Soskin //Tr. GOIN 1962. - Issue. 70, - S. 56-68.

78. Reference book on the climate of the USSR. JL: Hydrometeorological Publishing House, 1966 - Issue. 6 h. III. - 92 p.

79. Sustavov, Yu.V. Research of wind currents of the Baltic Sea on the basis of a mathematical model of the interaction of boundary layers / Yu.V. Sustavov, E.S. Chernyshova, I.E. Tsuprova// Tr. GOIN 1982. - Issue. 157. - S. 29-43.

80. Temnikova, I.P. Experience of climatic zoning of the Gulf of Riga / I.P. Temnikova // Meteorology and hydrology. 1972. - No. 7. - S. 108-114.

81. Tkach, A.V. Anthropogenic impact on the nutrition of fish larvae in the Sevastopol Bay / A.V. Weaver // Tez. report V All-Union Conference on the early ontogenesis of fish, Astrakhan, 1-3 Oct. 1991-M., 1991.-S. 155-157.

82. Tupikin, S.N. Types and trajectories of storm cyclones in the southern Baltic / S.N. Tupikin // Abstracts of reports. section 37th Congress of the Geographical Society of the USSR, dedicated. Modern problems of studying the World Ocean, Frunze, 1980. P.41-51.

83. Tupikin, S.N. Typification of storm cyclone trajectories for the southern part of the Baltic Sea / S.N. Tupikin // Regime-forming factors, hydrometeorological and hydrochemical processes in the seas of the USSR. L .: Gidrometeoizdat, 1988. - S. 260-269.

84. Tylik, K.V. Ichthyofauna of the Kaliningrad region / K.V. Tylik. Reference manual Kaliningrad: Publishing house of KSTU, 2003. - 128 p.

85. Khandozhko, JI.A. Typical trajectories of storm cyclones for the northwest ETC / L.A. Khandozhko //Tr. LGMI, 1964. - Issue. 22. - S. 54-61.

86. Hupfer, P. Baltika. Small sea big problems / P. Hupfer. - L.: Gidrometeoizdat, 1982. - 135 p.

87. Tsverava, V.G. Storms on the Baltic Sea and their connection with the ESP / V.G. Tsverava //Tr.GGO. -1965. Issue. 149. - S. 46-52.

88. Zirgoffer, A. The Atlantic Ocean and its seas / A. Zirgoffer. -M.: Gidrometeoizdat, 1975. 350 p.

89. Shibaev, S.V. System analysis in fisheries research / S.V. Shibaev. Kaliningrad: KSTU, 2004. - 315 p.

90. Anon. Report of the working group on assessment of pelagic stocks in the Baltic / ICES С.М./ Assess. 1991,-18 p.

91. Anon. Systematic list of Estonian fishes. World Wide Web Electronic Publication, 14 January 2000. http://www.fishbase.org., version (10/2004).

92. Arias, A. Estados juveniles de la ictiofauna en las canos de las salinas de la bahia de Cadiz. Institute de Ciencias Marinas de Andalucia / A. Arias and P. Drake // CSIC, 1990. -20 p.

93 Collette, B.B. Family Belonidae Bonaparte 1832 needlefishes / B.B. Collette // Calif. Acad. sci. Annotated Checklists of Fishes, 2003. - No. 16.-22 p.m.

94 Collette, B.B. Belonidae / B.B. Collette, N.V. Parin; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau J. Nielsen and E. Tortonese (eds,) // Fishes of the north-eastern Atlantic and the Mediterranean, Unesco, Paris, 1986. Vol. 2. - P. 604-609.

95. Cooper, J.A. and F. Chapleau. Monophyly and intrarelationships of the family Pleuronectidae (Pleuronectiformes), with a revised classification / J.A. Cooper, F. Chapleau // Fish. Bull., 1998. No. 96(4). - P. 686-726.

96. Dawson, C.E. Syngnathidae. /C.E Dawson; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau, J. Nielsen and E. Tortonese (eds.) // Fishes of the north-eastern Atlantic and the Mediterranean. UNESCO, Paris, 1986. Vol. 2. - P. 628-639.

97. Defant, F. Klimat und Wetter der Ostsee / F. Defant // Kiel.Meeresforshugen. 1972.-Vol. 28, No.l. - P. 1-30.

98. Defant, F. Synoptik und Energetic der Hauberger Sturmflugwetteriage von Februars 1962 / F. Defant // Energetisha Analyze und Berechnung des Windfeldes// Offenbach-am-Main., 1972.-35 p.

99. Didzis, U. The structure and dynamics of fish communities in the Latvian coastal zone (Pape-Perkone), Baltic Sea / U. Didzis, E. Urtanas, A. Minde, D. Uzars // Acta Universitatis Latviensis. 2003. - Vol. 662.-P. 33-44.

100. Dubicka, M. Esguisse du dimat de la Pologne / M. Dubicka // Hommes et terres Nord., 1982.-No. 2.-P. 3-12.

101. Electronic World Wide Web publication. Fishbase, 2004. R. Froese and D. Pauly (Eds.), http://www.fishbase.org., version (10/2004).

102Fonzelius, S.N. Hydrography of the Baltic Deep Basins III / S.N. Fonzelius //Fish.Bd.Swed. Ser. Hydrogr., 1969. No. 23. - 97p.

103. Frank, H. Zur jahresseitlichen Vareation des thermohalinen Geschehens imwestlichen Bornholmbecken / H. Frank //Beitr. Meerreskunde, 1985. No. 53. - P. 3-16.

104. Frimodt, C. Multilingual illustrated guide to the world's commercial coldwater fish / C. Frimodt // Fishing News Books, Osney Mead, Oxford, England, 1995. 215 p.

105. Halbeisen, H.-W. Bestimmungsschlussel fur Fischlarven der Nordsee und angrenzender Gebiete / H.-W. Halbeisen // Institut fur Meereskunde, Dusternbrooker Weg 20, Kiel, Germany, 1988. 58 p.

106. Hela, I. Secular changes in the salinity of the upper waters of the Northern Baltic Sea / I. Hela //Comm.Phys.-Math.Soc.Sci Fennica. 1966. - Vol. 31. - No. bl4. -21p.

107. Hupfer, P. Meeresklimatische Veranderungen im Gebiet der 1900 / P. Hupfer //Veroff. Geoph.Inst.Leipzig-Berlin, 1962. Bd. 17. - H. 4. - P. 355-512.

108. Jones, A. Sexual maturity, fecundity and growth of the turbot, Scophthalmus maximus L. / A. Jones // J. Mar. Biol. Assoc. U.K., 1974. No. 54. - P. 109-125.

109. Kaiser, W. Zur Ursache der zeitlichen und raumlichen Differenzen des Beganns der Phytoplanktonblute in der Ostsee / W. Kaiser, S. Schulz // Fischerei-Forsch., 1976. No. 14. -P. 77-81.

110. Karasiova, E. Historical ichthyoplankton researches in the Baltic sea and their importance to the analysis of fish stocks of long-term dynamics / E. Karasiova // History of oceanography: Abstracts of the VII International Congress of the History of

111. Oceanography / General Editor V. L. Stryuk. Kaliningrad: Kaliningrad University Press, 2003.-P. 439-441.

112. Karasiova, E.M. Invasion and distribution of Cercopages pengoi in the Baltic Sea as an indicator of climatic changes / E.M. Karasiova, V.M Ivanovich, E.A. Gribov // ICES CM 2004/L:05. P. 26-28.

113. Karasiova, E.M. Fish larvae assemblages in the coastal shallow zone of the South -Eastern Baltic Sea: environmental factors driving interannual variability / E.M. Karasiova, E.A. Gribov, V.M. Andreeva//ICES CM2002/0:11.-P. 14-15.

114. Kaszmaruk, B. Okreslenia prawdopodobienstwa wystopowania wiatrow silnych I sztormow wellug dni w strefie palskieso wybzeza Baltiku / B. Kaszmaruk //Zesz.nauk. A.R.Szezecinie, 1973. -No.40. P. 157-162.

115. Klinkhardt, M. Zur Zytogenetik von Platichthys flesus und Limanda limanda (Pleuroectidae, Teleostei) und Karyoevolution der Pleuronectiformes / M. Klinkhardt // Z. Fischkunde, 1993. No. 2. - P. 65-75.

116. Kowalik, Z. Density currents in the Baltic Sea / Z. Kowalik, S. Taranowska //Ocea-nologia (PNR), 1974. Vol. 3 - P. 5-31.

117. Knijn, R.J. Atlas of North Sea fishes / R.J. Knijn, T.W. Boon, H.J.L. Heessen, J.R.G. Hislop // International Council for the Exploration of the Sea, Copenhagen, Denmark, 1993, - 268 p.

118. Laska, M. Spektral analisys of the periodic water lewel changes in the Baltic / M.Laska / /Intern. Hydrolog. Rev., 1969. No. 46. ​​- 156 p.

119. Matthaus, W. Langzeittrends der Dichte im Gotlandbecken / W. Matthaus //Beitr.Meereskunde, 1983. H. 48. - P. 47-56.

120. Maug6, L.A. Gobiidae. / L.A. mauge; In J. Daget, J.-P. Gosse and D.F.E. Thys van den Audenaerde (eds.) // Check-list of the freshwater fishes of Africa (CLOFFA). ISNB, Brussels; MRAC, Tervuren; and ORSTOM, Paris, 1986. Vol. 2. - P. 358-388.

121. Miller, P.J., Gobiidae./ P.J. Miller; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau, J. Nielsen and E. Tortonese (eds.) // Fishes of the North-eastern Atlantic and the Mediterranean. Volume 3. UNESCO, Paris, 1986. P. 1019-1085.

122 Muus, B.J. Seafish / B.J. Muus, J.G. Nielsen // Scandinavian Fishing Year Book, Hedehusene, Denmark, 1999. 340 p.

123. Muus, B.J. Collins guide to the sea fishes of Britain and North-Western Europe / B.J. Muusand, P. Dahlstrom // Collins, London, UK, 1974. 244 p.

124 Muus, B.J. Meeresfische der Ostsee, der Nordsee, des Atlantiks / B.J. Muus, P. Dahlstrom // BLV Verlagsgesellschaft, Miinchen, 1978. 244 p.

125. Nankee, R. L. Observations of deformed fish larvae in Long Island Sound and Niantic Bay, Connecticut / R.L. Nankee // Rapp. P. v. Reun. Cons. int. Explore. Mer. 178, 1981.-p. 355-356.

126. Nielsen, J.G. Pleuronectidae / J.G. Nielsen; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau, J. Nielsen and E. Tortonese (eds.) // Fishes of the North-eastern Atlantic and the Mediterranean. UNESCO, Paris, 1986. Vol. 3. - P. 1299-1307.

127. Ojaveer, E. Baltic herring, Clupea harengus membras L. / E. Ojaveer, E. Pihu and T. Saat (eds.) // Fishes of Estonia. Estonian Academy Publishers, Tallinn, 2003. P. 58-79.

128 Reay, P.J. Ammodytidae / P.J. Ray; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau, J. Nielsen and E. Tortonese (eds.) // Fishes of the north-eastern Atlantic and the Mediterranean. UNESCO, Paris, 1986. Vol. 2. - P. 945-950.

129. Riede, K. Global register of migratory species from global to regional scales. Final Report of the R&D-Projekt 808 05 081 / K. Riede // Federal Agency for Nature Conservation, Bonn, Germany, 2004. - 329 p. + appendix.

130 Stein, D.L. Liparididae / D.L. Stein, K.W. Able; In P.J.P. Whitehead, M.-L. Bauchot, J.-C. Hureau, J. Nielsen and E. Tortonese (eds.) // Fishes of the North-eastern Atlantic and the Mediterranean. UNESCO, Paris, 1986. Vol. III. - P. 1275-1283.

131. Winkler, H.M. Checklist and status of fish species in the Baltic Sea / H.M. Winkler, K. Skora, R. Repecka, M. Ploks, A. Neelov, L. Urho, A. Gushin, H. Jespersen. // ICES CM 2000/Mini:ll. -15p.

132. Zander, C. D. Zur Bedeutung von Kleinfischen in Okosestemen der Ostsee / Von C. D. Zander // Seevogel, 1988. Band 9, Helt 4. - P. 51-55.

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Deeply cut into the land, the Baltic Sea has a very complex outline of the coast and forms large bays: Bothnian, Finnish and Riga. This sea has almost everywhere land borders, and only from the Danish Straits (Great and Small Belt, Sound, Farman Belt) it is separated by conditional lines passing between certain points on their coasts. Due to the peculiar regime, the Danish Straits do not belong to the Baltic Sea. They link it to the North Sea and through it to the Atlantic Ocean. The depths above the rapids separating the Baltic Sea from the straits are small: above the Darser threshold - 18 m, above the Drogden threshold - 7 m. The cross-sectional area in these places is 0.225 and 0.08 km 2, respectively. The Baltic Sea is weakly connected with the North Sea and has limited water exchange with it, and even more so with the Atlantic Ocean.

It belongs to the type of inland seas. Its area is 419 thousand km 2, volume - 21.5 thousand km 3, average depth- 51 m, greatest depth- 470 m.

Bottom relief

The bottom relief of the Baltic Sea is uneven. The sea lies entirely within the shelf. The bottom of its basin is indented by underwater depressions, separated by hills and socles of islands. In the western part of the sea there are shallow Arkon (53 m) and Bornholm (105 m) depressions, separated by about. Bornholm. IN central regions In the sea, quite extensive spaces are occupied by the Gotland (up to 250 m) and Gdansk (up to 116 m) basins. North of about. Gotland lies the Landsort Depression, where the greatest depth of the Baltic Sea is recorded. This depression forms a narrow trench with depths of more than 400 m, which stretches from the northeast to the southwest, and then to the south. Between this trough and the Norrköping depression located to the south, an underwater hill stretches with depths of about 112 m. Further south, the depths again increase slightly. On the border of the central regions with the Gulf of Finland, the depth is about 100 m, with the Bothnian - about 50 m, and with the Riga - 25-30 m. The bottom relief of these bays is very complex.

Bottom relief and currents of the Baltic Sea

Climate

The climate of the Baltic Sea is of maritime temperate latitudes with features of continentality. The peculiar configuration of the sea and a significant length from north to south and from west to east create differences in climatic conditions in different areas of the sea.

The Icelandic low, as well as the Siberian and Azores anticyclones, most significantly affect the weather. The nature of their interaction determines the seasonal features of the weather. In autumn and especially in winter, the Icelandic Low and the Siberian High interact intensively, which intensifies cyclonic activity over the sea. In this regard, in autumn and winter, deep cyclones often pass, which bring with them cloudy weather with strong southwestern and western winds.

In the coldest months - January and February - average temperature air temperature in the central part of the sea is -3° in the north and -5-8° in the east. With rare and short-term intrusions of cold Arctic air associated with the strengthening of the Polar High, the air temperature over the sea drops to -30° and even to -35°.

In the spring-summer season, the Siberian High collapses, and the Baltic Sea is affected by the Icelandic Low, the Azores and, to some extent, the Polar High. The sea itself is located in a zone of low pressure, along which cyclones from the Atlantic Ocean are less deep than in winter. In this regard, in spring the winds are very unstable in direction and low in speed. Northerly winds are responsible for the usually cold spring in the Baltic Sea.

In summer, predominantly western, northwestern and southwestern weak to moderate winds blow. They are associated with the cool and humid summer weather characteristic of the sea. The average monthly temperature of the warmest month - July - is 14-15° in the Gulf of Bothnia and 16-18° in other areas of the sea. Hot weather is rare. It is caused by short-term inflows of warm Mediterranean air.

Hydrology

About 250 rivers flow into the Baltic Sea. The largest amount of water is brought per year by the Neva - an average of 83.5 km 3, the Vistula - 30 km 3, the Neman - 21 km 3, the Daugava - about 20 km 3. The runoff is unevenly distributed across the regions. So, in the Gulf of Bothnia it is 181 km 3 /year, in Finland - 110, in Riga - 37, in the central part of the Baltic - 112 km 3 /year.

Geographical position, shallow water, complex bottom topography, limited water exchange with the North Sea, significant river runoff, and climate features have a decisive influence on hydrological conditions.

The Baltic Sea is characterized by some features of the eastern subtype of the subarctic structure. However, in the shallow Baltic Sea, it is represented mainly by surface and partially intermediate waters, significantly transformed under the influence of local conditions (limited water exchange, river runoff, etc.). The water masses that make up the structure of the waters of the Baltic Sea are not identical in their characteristics in different areas and change with the seasons. This is one of the distinguishing features of the Baltic Sea.

Water temperature and salinity

In most areas of the Baltic Sea, surface and deep water masses are distinguished, between which lies a transitional layer.

Surface water (0-20 m, in some places 0-90 m) with a temperature of 0 to 20°C, a salinity of approximately 7-8‰ is formed in the sea itself as a result of its interaction with the atmosphere (precipitation, evaporation) and with the waters of the continental runoff. This water has winter and summer modifications. In the warm season, a cold intermediate layer is developed in it, the formation of which is associated with a significant summer heating of the sea surface.

The temperature of deep water (50-60 m - bottom, 100 m - bottom) - from 1 to 15 °, salinity - 10-18.5‰. Its formation is associated with the entry of deep waters into the sea through the Danish straits and with mixing processes.

The transitional layer (20-60 m, 90-100 m) has a temperature of 2-6°C, salinity of 8-10‰, and is formed mainly by mixing surface and deep waters.

In some areas of the sea, the structure of the waters has its own characteristics. For example, in the Arkon region, there is no cold intermediate layer in summer, which is explained by the relatively shallow depth of this part of the sea and the influence of horizontal advection. The Bornholm region is characterized by a warm layer (7-11°) observed in winter and summer. It is formed by warm waters coming here from the slightly warmer Arkona basin.

In winter, the water temperature is somewhat lower near the coast than in the open parts of the sea, while it is slightly higher near the western coast than near the eastern one. Thus, the average monthly water temperature in February near Ventspils is 0.7°, at the same latitude in the open sea - about 2°, and near the western coast - 1°.

Water temperature and salinity at the surface of the Baltic Sea in summer

Summer temperature surface water is not the same in different areas of the sea.

The decrease in temperature near the western shores, in the central and southern regions is explained by the predominance of westerly winds, which drive the surface layers of water away from the western shores. Colder underlying waters rise to the surface. In addition, a cold current from the Gulf of Bothnia passes along the Swedish coast to the south.

Clearly pronounced seasonal changes in water temperature cover only the upper 50-60 m; deeper, the temperature changes very little. In the cold season, it remains approximately the same from the surface to the horizons of 50-60 m, and deeper it drops somewhat to the bottom.

Water temperature (°C) on a longitudinal section in the Baltic Sea

In the warm season, the increase in water temperature as a result of mixing extends to horizons of 20–30 m. From there, it abruptly decreases to horizons of 50–60 m and then again rises somewhat towards the bottom. The cold intermediate layer persists in summer, when the surface layer warms up and the thermocline is more pronounced than in spring.

Limited water exchange with the North Sea and significant river runoff result in low salinity. On the sea surface, it decreases from west to east, which is associated with the predominant inflow river waters to the eastern part of the Baltic. In the northern and central regions of the basin, salinity decreases somewhat from east to west, since in cyclonic circulation, saline waters are transported from south to northeast along east coast sea ​​further than along the western. A decrease in surface salinity can also be traced from south to north, as well as in bays.

In the autumn-winter season, the salinity of the upper layers slightly increases due to a decrease in river runoff and salinization during ice formation. In spring and summer, salinity on the surface decreases by 0.2-0.5‰ compared to the cold half-year. This is explained by the desalination effect of continental runoff and the spring melting of ice. Almost throughout the sea, a significant increase in salinity from the surface to the bottom is noticeable.

For example, in the Bornholm Basin, salinity at the surface is 7‰ and about 20‰ at the bottom. The change in salinity with depth is basically the same throughout the sea, with the exception of the Gulf of Bothnia. In the southwestern and partly central regions of the sea, it gradually and slightly increases from the surface to horizons of 30-50 m, below, between 60-80 m, there is a sharp layer of a jump (halocline), deeper than which the salinity again slightly increases towards the bottom. In the central and northeastern parts, salinity increases very slowly from the surface to 70–80 m horizons; deeper, at 80–100 m horizons, there is a halo wedge, and then salinity slightly increases to the bottom. In the Gulf of Bothnia, salinity increases from the surface to the bottom by only 1-2‰.

In autumn-winter time, the flow of North Sea waters into the Baltic Sea increases, and in summer-autumn it somewhat decreases, which leads to an increase or decrease in the salinity of deep waters, respectively.

In addition to seasonal fluctuations in salinity, the Baltic Sea, unlike many seas of the World Ocean, is characterized by its significant interannual changes.

Observations of salinity in the Baltic Sea from the beginning of this century until recent years show that it tends to increase, against which short-term fluctuations appear. Changes in salinity in the basins of the sea are determined by the inflow of water through the Danish Straits, which in turn depends on hydrometeorological processes. These include, in particular, the variability of large-scale atmospheric circulation. The long-term weakening of cyclonic activity and the long-term development of anticyclonic conditions over Europe lead to a decrease in precipitation and, as a consequence, to a decrease in river runoff. Changes in salinity in the Baltic Sea are also associated with fluctuations in the values ​​of continental runoff. With a large river runoff, the level of the Baltic Sea slightly rises and the sewage flow from it intensifies, which in the shallow zone of the Danish Straits (the smallest depth here is 18 m) limits the access of salt water from the Kattegat to the Baltic. With a decrease in river flow, saline waters more freely penetrate into the sea. In this regard, fluctuations in the inflow of saline waters into the Baltic are in good agreement with changes in the water content of the rivers of the Baltic basin. IN last years an increase in salinity is noted not only in the bottom layers of the basins, but also in the upper horizons. At present, the salinity of the upper layer (20-40 m) has increased by 0.5‰ compared to the average long-term value.

Salinity (‰) on a longitudinal section in the Baltic Sea

Salinity variability in the Baltic Sea is one of the most important factors regulating many physical, chemical and biological processes. Due to the low salinity of the surface waters of the sea, their density is also low and decreases from south to north, varying slightly from season to season. Density increases with depth. In the areas of distribution of saline Kattegat waters, especially in basins at the horizons of 50-70 m, a constant layer of a density jump (pycnocline) is created. Above it, in the surface horizons (20-30 m), a seasonal layer of large vertical density gradients is formed, due to a sharp change in water temperature at these horizons.

Water circulation and currents

In the Gulf of Bothnia and in the shallow area adjacent to it, a density jump is observed only in the upper (20-30 m) layer, where it is formed in spring due to freshening by river runoff, and in summer due to heating of the surface layer of the sea. A permanent lower layer of the density jump is not formed in these parts of the sea, since deep saline waters do not penetrate here and year-round stratification of waters does not exist here.

Water circulation in the Baltic Sea

The vertical distribution of oceanological characteristics in the Baltic Sea shows that in the southern and central regions the sea is divided by a density jump layer into upper (0-70 m) and lower (from 70 m to the bottom) layers. In late summer - early autumn, when weak winds prevail over the sea, wind mixing extends to horizons of 10-15 m in the northern part of the sea and to horizons of 5-10 m in the central and southern parts and serves as the main factor in the formation of the upper homogeneous layer. During autumn and winter, with an increase in wind speeds over the sea, mixing penetrates to horizons of 20–30 m in the central and southern regions, and up to 10–15 m in the east, since relatively weak winds blow here. As autumn cooling intensifies (October - November), the intensity of convective mixing increases. During these months, in the central and southern regions of the sea, in the Arkon, Gotland and Bornholm depressions, it covers a layer from the surface up to about 50-60 m. ) and is limited by the density jump layer. In the northern part of the sea, in the Gulf of Bothnia and in the west of the Gulf of Finland, where autumn cooling is more significant than in other areas, convection penetrates to horizons of 60-70 m.

The renewal of deep waters, the sea occurs mainly due to the inflow of the Kattegat waters. With their active inflow, the deep and bottom layers of the Baltic Sea are well ventilated, and with small amounts of salt water flowing into the sea, great depths stagnation occurs in the depressions up to the formation of hydrogen sulfide.

The strongest wind waves are observed in autumn and winter in open, deep areas of the sea with prolonged and strong southwestern winds. Stormy 7-8-point winds develop waves up to 5-6 m high and 50-70 m long. In the Gulf of Finland, strong winds of these directions form waves 3-4 m high. In the Gulf of Bothnia, storm waves reach a height of 4-5 m. big waves come in November. In winter, with more strong winds the formation of high and long waves is prevented by ice.

As in other seas of the northern hemisphere, the surface circulation of the Baltic Sea has a general cyclonic character. Surface currents are formed in the northern part of the sea as a result of the confluence of waters emerging from the Gulf of Bothnia and the Gulf of Finland. The general flow is directed along the Scandinavian coast to the southwest. Going around on both sides about. Bornholm, he is heading through the Danish Straits to the North Sea. At the southern coast, the current is directed to the east. Near the Gulf of Gdansk, it turns north and moves along the eastern coast to about. Khnum. Here it branches into three streams. One of them goes through the Irben Strait to the Gulf of Riga, where, together with the waters of the Daugava, it creates a circular current directed counterclockwise. Another stream enters the Gulf of Finland and spreads along its southern coast almost to the mouth of the Neva, then turns to the northwest and, moving along north coast, along with the river waters out of the bay. The third flow goes to the north and through the straits of the Aland skerries penetrates into the Gulf of Bothnia. Here, along the Finnish coast, the current rises to the north, goes around the northern coast of the bay and descends to the south along the coast of Sweden. In the central part of the bay, there is a closed circular counterclockwise current.

The speed of the permanent currents of the Baltic Sea is very low and is approximately 3-4 cm/s. Sometimes it increases to 10-15 cm/s. The current pattern is very unstable and is often disturbed by the wind.

The prevailing wind currents in the sea are especially intense in autumn and winter, and during strong storms their speed can reach 100-150 cm/s.

Deep circulation in the Baltic Sea is determined by the flow of water through the Danish straits. The inlet current in them usually passes to horizons of 10-15 m. Then this water, being denser, descends into the underlying layers and is slowly transported by the deep current, first to the east and then to the north. With strong westerly winds, water from the Kattegat flows into the Baltic Sea almost along the entire cross section of the straits. East winds, on the contrary, increase the outlet current, which extends to the horizons of 20 m, and the inlet current remains only near the bottom.

Due to the high degree of isolation from the World Ocean, the tides in the Baltic Sea are almost invisible. Fluctuations in the level of the tidal character in individual points do not exceed 10-20 cm. The average sea level experiences secular, long-term, inter-annual and intra-annual fluctuations. They can be associated with a change in the volume of water in the sea as a whole and then have the same value for any point in the sea. The secular level fluctuations (except for changes in the volume of water in the sea) reflect the vertical movements of the shores. These movements are most noticeable in the north of the Gulf of Bothnia, where the rate of land rise reaches 0.90-0.95 cm/year, while in the south the rise is replaced by the sinking of the coast at a rate of 0.05-0.15 cm/year.

In the seasonal course of the Baltic Sea level, two minima and two maxima are clearly expressed. The lowest level is observed in spring. With the arrival of spring flood waters, it gradually rises, reaching a maximum in August or September. After that, the level goes down. The secondary autumn low is coming. With the development of intense cyclonic activity, westerly winds drive water through the straits into the sea, the level rises again and reaches a secondary, but less pronounced maximum in winter. The height difference between the summer maximum and the spring minimum is 22-28 cm. It is greater in the bays and less in the open sea.

Surge fluctuations in the level occur quite quickly and reach significant values. In open areas of the sea, they are approximately 0.5 m, and at the tops of bays and bays they are 1-1.5 and even 2 m. -26 h. Level changes associated with seiches do not exceed 20-30 cm in the open part of the sea and reach 1.5 m in the Neva Bay. Complex seiche level fluctuations are one of the characteristic features of the Baltic Sea regime.

The catastrophic St. Petersburg floods are connected with sea level fluctuations. They occur when the level rise is due to the simultaneous action of several factors. Cyclones that cross the Baltic Sea from the southwest to the northeast cause winds that drive water from western regions sea ​​and overtake it in the north-eastern part of the Gulf of Finland, where the sea level rises. Passing cyclones also cause seiche fluctuations in the level, at which the level rises in the Aland region. From here, a free seiche wave, driven by western winds, enters the Gulf of Finland and, together with the surge of water, causes a significant increase (up to 1-2 m and even 3-4 m) in the level at its top. This prevents the flow of the Neva water into the Gulf of Finland. The water level in the Neva is rapidly rising, which leads to floods, including catastrophic ones.

ice coverage

The Baltic Sea is covered with ice in some areas. The earliest (around the beginning of November) ice forms in the northeastern part of the Gulf of Bothnia, in small bays and off the coast. Then the shallow areas of the Gulf of Finland begin to freeze. The maximum development of the ice cover reaches in early March. By this time, motionless ice occupies the northern part of the Gulf of Bothnia, the region of the Aland skerries and the eastern part of the Gulf of Finland. Floating ice occurs in the open areas of the northeastern part of the sea.

The distribution of fixed and floating ice in the Baltic Sea depends on the severity of the winter. Moreover, in mild winters, ice, having appeared, may completely disappear, and then appear again. In severe winters, the thickness of immobile ice reaches 1 m, and floating ice - 40-60 cm.

Melting begins in late March - early April. The release of the sea from ice goes from the southwest to the northeast.

Only in severe winters in the north of the Gulf of Bothnia, ice can be found in June. However, the sea is cleared of ice every year.

Economic importance

Freshwater fish species live in the significantly freshened waters of the bays of the Baltic Sea: crucian carp, bream, chub, pike, etc. There are also fish that spend only part of their lives in fresh waters, the rest of the time they live in the salty waters of the sea. These are now rare Baltic whitefish, typical inhabitants of the cold and clean lakes of Karelia and Siberia.

A particularly valuable fish is the Baltic salmon (salmon), which forms an isolated herd here. The main habitats of salmon are the rivers of the Gulf of Bothnia, the Gulf of Finland and the Gulf of Riga. She spends the first two or three years of her life mainly in the southern part of the Baltic Sea, and then goes to spawn in the rivers.

Purely marine fish species are common in the central regions of the Baltic, where salinity is relatively high, although some of them also enter fairly fresh bays. For example, herring lives in the Gulf of Finland and Riga. More saltwater fish - Baltic cod - do not enter the fresh and warm bays. Eel is a unique species.

In fishing, the main place is occupied by herring, sprat, cod, river flounder, smelt, perch and various types of freshwater fish.

Edition: Nauka, Moscow, 2009, 379 pages, ISBN: 978-5-02-025361-2

Language(s) Russian

In the composition of the igneous provinces of the northeastern part of the Baltic Shield, manifestations of dike magmatism occupy a significant place both in terms of the volume of intruded melts and in terms of their occurrence. As a rule, kid swarms mark large stages of activation of plume-lithospheric processes that occurred either during the restructuring of the basement of Fennoscandia or in adjacent territories. In the latter case, dikes associated with distant tectonic events are very rare, but their role in assessing the scale and nature of tectonomagmatic processes is significant. In the Kola region, the study of dike magmatism was carried out locally and was associated with the study of the intrusive activity of certain stages of the evolution of the Baltic Shield or with the study of the magmatism of a particular structure. Despite the significant progress in intrusive petrology, the problems of dike magmatism can without exaggeration be classified as the most difficult to solve. Let us name at least three reasons complicating the study of dikes.

First, the spatial disunity of small bodies and swarms scattered over a vast area leads to the fact that geologists are forced to organize costly field studies of large areas, conducting large-scale mapping of dike development regions remote from each other and, as a result, obtaining data on only a few geological objects. More often, the study of dike magmatism is carried out along the way, in the course of the study of other intrusive bodies. In this case, data is collected over many field seasons. It is in this way that factual material was collected for the present work, which summarizes the results of the authors for more than thirty years of research on the dikes of the region.

Secondly, in order to correlate dike swarms and elucidate the nature of relationships between subvolcanic and plutonic manifestations of magmatism, it is necessary to determine the age of each dike, or at least an individual swarm. Unfortunately, large-scale isotope studies are unlikely to be possible in the foreseeable future. Given the above, we tried to make the maximum number of determinations of the absolute age of laika rocks using Rb-Sr, U-Pb, 40Ar/39Ar and Sm-Nd methods. Already the first dates obtained made it possible for the first time to identify manifestations of the Grenville stage of tectonomagmatic activation on the territory of the Kola region, as well as to outline the area of ​​development of Paleozoic dolerite dikes.

Thirdly, since a dike is an independent intrusive body, the question of the need to determine the chemical composition of each dike and to estimate the contents of trace elements in its rock is of particular relevance. The task is complicated by the presence of zoning in dikes, the presence of xenogenic material in them, and the manifestation of processes of contamination by the material of host rocks.

Thus, a systematic study of dike magmatism required much greater expenditures both for the organization of field work and for analytical studies. In this paper, for the first time, we tried to summarize all the currently available factual data on laik magmatism, accumulated by the authors in the course of more than 30 years of studying the Precambrian (Zh.A. Felotov - Zh.A.F.) and Paleozoic (A.A. Arzamastsev - A.A.A., L.V. Arzamastseva) dikes. The work also uses primary materials collected by the authors in the course of joint work with industrial geological organizations.

Material on the dikes of the Khibiny massif was collected by one of the authors (A.A.A.) in the course of a joint project of the Geological Institute of the KSC RAS ​​and the Khibinogorsk GRP of the Murmansk GRE PGO "Sevzapgeologiya" (V.A. Kaverina) (1986-1988).

The material on manifestations of kimberlite magmatism was obtained (A.A.A.) in the course of joint work of the Geological Institute of the KSC RAS ​​and the Central Kola State Geological Survey (M.M. Kalinkin, I.V. Polyakov) (1991-1993).

The material on the framing dikes of the Ivanovo volcano-plutonic complex was obtained during joint studies of the Geological Institute of the KSC RAS ​​(A.A.A.) and the experimental-methodological batch of the Kola complex geological survey of ultra-deep drilling PGO "Nedra" (M.S. Rusanov, V.I. Khmelinsky) (1985-1989).

Material on the composition and distribution of dikes in the area of ​​the northern framing of the Keiv and Kolmozero-Voronya structures was obtained in the course of joint research by the Geological Institute of the KSC RAS ​​(Zh.A.F.) and the Central Kola State Geological Survey (A.P. Lipov) (1979-1981) .

The material on dikes of the East Murmansk coast was collected in the course of joint work of the Geological Institute of the KSC RAS ​​(Zh.A.F.) and the mineralogical party of the Central Kola State Geological Survey (S.S. Karavaev) (1988-1991).

The distribution of dikes in the rest of the area of ​​the Kola region was estimated according to the reports of the geological survey crews of the Central Kola Geological Survey. The collections of thin sections of dike rocks collected by production organizations were studied by us in the museum of Murmangeolkom in Apatity. In addition, the collection of thin sections of dike rocks of Academician A.A. Polkanov, kept at the Department of Petrography of the Geological Faculty of St. Petersburg University, was examined.

Most of the analytical work was carried out in the laboratories of the Geological Institute of the KSC RAS ​​(Ya.A. Pakhomovskii, L.I. Koval). Precision studies of the composition of minerals (LA-ICP-MS) and rocks (1CP-MS) were carried out jointly with professors Fernando Bea and Pilar Montero (University of Granada, Spain). Isotopic and geochronological studies were carried out jointly with B.V. Belyatsky (Institute of Geology and Geochronology of the Precambrian RAS) and A.V. Travin (Analytical Center of the Joint Institute of Geology, Geophysics and Mineralogy, Siberian Branch of the Russian Academy of Sciences). Part of the isotope determinations of Proterozoic dikes was made by Yu.V. Amelin (Institute of Precambrian Geology and Geochronology, Russian Academy of Sciences). Great help in preparing the manuscript for publication was provided by S.E. Tsarev and T. Smarchuk. The authors express their deep gratitude to all the above colleagues.

The work was carried out within the framework of the priority programs of the ONZ RAS 6 and 8, and was also financed by the Russian Foundation for Basic Research (grants 09-05-00224a

The Baltic Sea washes the shores of the Russian Federation, Denmark, and the Baltic countries. The Russian Federation owns small water areas in the eastern part of the Baltic Sea - the Kaliningrad Bay and part of the Curonian Lagoon (the territory of the Kaliningrad Region) and the eastern outskirts of the Gulf of Finland (the territory of the Leningrad Region).

The Baltic Sea is deeply incised into the northwestern part of Eurasia. This is an inland sea, connected to the North Sea of ​​the Atlantic Ocean by the system of the Øresund (Sund), Great Belt, Small Belt straits, known collectively as the Danish Straits. They pass into the deep and wide straits of the Skagerrak, Kattegat, which already belong to the North Sea, which is directly connected with.

The area of ​​the Baltic Sea is 419 thousand km2, the volume is 21.5 thousand km3, the average depth is 51 m, the greatest depth is 470 m.

About 250 rivers flow into the Baltic Sea. The largest rivers are Vistula, Oder, Neman, Daugava, Neva. The Neva brings the largest amount of water per year - an average of 83.5 km3.
The Baltic Sea stretches from the southwest to the northeast, and its greatest length is 1360 km. The widest point of the sea is at 60° N. sh., between St. Petersburg and Stockholm, it stretches for almost 650 km.

The bottom relief of the Baltic Sea is uneven. The sea lies entirely within the shelf. The bottom of its basin is indented by underwater depressions, separated by hills and socles of islands.

The Baltic Sea is characterized by a long coastline. It has many bays, bays and a large number of islands. The sea is a collection of individual basins: the zone of the Danish Straits, the open or central part of the sea and three large bays - Bothnian, Finnish and Riga, which account for almost half of the sea.

Numerous islands of the Baltic Sea are located both off the mainland coast and in the open sea; in some parts of the sea the islands are grouped in large archipelagos, in others they stand alone.


The largest of the islands: Danish - Zealand, Fyn, Lolland, Falster, Langeland, Mön, Bornholm; Swedish - Gotland, Eland; German - Rügen and Fehmarn; - Saaremaa and Hiiumaa.

The coasts of the northern and southern half of the sea differ sharply in character. The skerry shores of Sweden and Finland are indented with small bays and gulfs, framed by islands composed of crystalline rocks. They are mostly low, sometimes naked, and in some places overgrown with coniferous forest. southern shores low-lying, composed of sand and have a large number of shallows. In some places, along the coast, chains of sand dunes stretch here, and long spits protrude into the sea, forming large lagoons desalinated by the flow of rivers. The largest of these shallow bays are Curonian and Vistula.


The bottom sediments of the Baltic Sea are represented mainly by silts and sand. The soils of the Baltic Sea are characterized by stones and boulders, often found at the bottom of the sea. Sandy deposits are common in coastal areas. In the Gulf of Finland most of The bottom is covered with sands with separate patches of silt, occupying small depressions and forming a field of sediments of the Neva river delta, somewhat elongated along the strike of the bay. Construction of a dam to protect high seas significant part of the water area, significantly changed the composition and distribution of precipitation that existed in natural conditions.

The climate of the Baltic Sea is of maritime temperate latitudes with features of continentality. The peculiar configuration of the sea and a significant length from north to south and from west to east create differences in climatic conditions in different areas of the sea.

The Icelandic low, as well as the Siberian and Azores anticyclones, most significantly affect the weather. The nature of their interaction determines the seasonal features of the weather. In autumn and especially in winter, the Icelandic Low and the Siberian High interact intensively, which intensifies cyclonic activity over the sea. In this regard, in autumn and winter, deep cyclones often pass, which bring with them cloudy weather with strong southwestern and western winds.

In the coldest months - January and February - the average in the central part of the sea is -3°С in the north and -5...-8°С in the east. With rare and short-term intrusions of cold Arctic air associated with the strengthening of the Polar High, the air temperature over the sea drops to –30°С and even to –35°С.

In summer, predominantly western, northwestern weak to moderate winds blow. They are associated with the cool and humid summer weather characteristic of the sea. The average monthly temperature of the warmest month is 14–15°C in the Gulf of Bothnia and 16–18°C in the rest of the sea. Hot weather is rare. It is caused by short-term inflows of warm Mediterranean air.


The temperature conditions of the waters of the Baltic Sea in different parts of it are not the same and depend not only on the geographical location of the place, but also on meteorological and hydrological features of this area. The heating of the surface by the rays of the sun, the runoff of river waters and the inflow of deep oceanic waters are of the greatest importance for the temperature regime of the Baltic Sea. This determines the general picture of the temperature conditions of the sea. In the surface layers, the water temperature varies widely. At depths exceeding 50 meters, the water temperature is kept within 3–4 ° C all year round in the southern part of the sea and near zero in the northern Bothnian region.

During the summer months, surface water temperatures are generally close to air temperatures. Near the eastern shores, the water temperature is higher due to the influence of warm, southward land masses, and along the western, Swedish, shores, it is lower due to the flow of cold waters from the north, from the Gulf of Bothnia. In winter, on the contrary, the eastern parts of the sea are colder than the western ones; they are subject to the influence of the chilled land masses of the mainland, and the western parts of the sea during this period experience a regular influx of warm air masses from the Atlantic.

Limited water exchange with the North Sea and significant river runoff result in low salinity. On the sea surface, it decreases from west to east, which is associated with the predominant inflow of river waters from the eastern Baltic. In the northern and central regions of the basin, salinity somewhat decreases from east to west, since in cyclonic circulation, saline waters are transported from south to northeast along the eastern coast of the sea further than along the western one. A decrease in surface salinity is also traced from south to north in the bays.

Almost throughout the sea, a significant increase in salinity from the surface to the bottom is noticeable. The change in salinity with depth is basically the same throughout the sea, with the exception of the Gulf of Bothnia. In the southwestern and partly central regions of the sea, it gradually and slightly increases from the surface to horizons of 30–50 m; below, between 60–80 m, there is a sharp shock layer (halocline), deeper than which the salinity again slightly increases towards the bottom. In the central and northeastern parts, salinity increases very slowly from the surface to horizons of 70–80 m; deeper, at 80–100 m, there is a halocline, and then salinity slightly increases to the bottom. In the Gulf of Bothnia, salinity increases from the surface to the bottom only by 1–2‰.

In autumn-winter time, the flow of North Sea waters into the Baltic Sea increases, and in summer-autumn it somewhat decreases, which leads to an increase or decrease in the salinity of deep waters, respectively. In the autumn-winter season, the salinity of the upper layers slightly increases due to reduction and deviation during ice formation. In spring and summer, salinity on the surface decreases by 0.2–0.5‰ compared to the cold half of the year. This is explained by the desalination effect of continental runoff and the spring melting of ice. In addition to seasonal fluctuations in salinity, the Baltic Sea, unlike many seas of the World Ocean, is characterized by its significant interannual changes. Salinity variability in the Baltic Sea is one of the most important factors regulating many physical, chemical and biological processes. Due to the low salinity of the surface waters of the sea, their density is also low and decreases from south to north, varying slightly from season to season. Density increases with depth.

The strongest wind waves are observed in autumn and winter in open, deep areas of the sea with prolonged and strong southwestern winds. Stormy 7–8-point winds develop waves up to 5–6 m high and 3–4 m long. The largest waves occur in November. In winter, with stronger winds, the formation of high and long waves is prevented by ice. As in other seas of the northern hemisphere, the surface circulation of the Baltic Sea has a general cyclonic character.



Surface currents are formed in the northern part of the sea as a result of the confluence of waters emerging from the Gulf of Bothnia and the Gulf of Finland. The speed of the permanent currents of the Baltic Sea is very low and is approximately 3–4 cm/s. Sometimes it increases to 10–15 cm/s. The current pattern is very unstable and is often disturbed by the wind. The wind currents prevailing in the sea are especially intense in autumn and winter, and during strong storms their speed can reach 100–150 cm/s.

Deep circulation in the Baltic Sea is determined by the flow of water through the Danish straits. The inlet current in them usually passes to a horizon of 10–15 m. Then this water, being denser, descends into the underlying layers and is slowly transported by the deep current, first to the east and then to the north.

Due to the high degree of isolation from the World Ocean, the tides in the Baltic Sea are almost invisible. Fluctuations in the tidal level at individual points do not exceed 10–20 cm. Two minimums and two maxima are clearly expressed in the seasonal course of the Baltic Sea level. The lowest level is observed in spring. With the arrival of spring flood waters, it gradually rises, reaching a maximum in August or September. After that, the level goes down. The secondary autumn low is coming. With the development of intense cyclonic activity, westerly winds drive water through the straits into the sea, the level rises again and reaches a secondary, but less pronounced maximum in winter. The difference in level heights between the summer maximum and the spring minimum is 22–28 cm. It is larger in bays and smaller in the open sea.

Surge fluctuations in sea level occur quite quickly and reach significant values. In the open areas of the sea, they are approximately 0.5 m, and at the tops of bays and bays they are 1–1.5 and even 2 m. h. Level changes associated with seiches do not exceed 20–30 cm in the open part of the sea and reach 1.5 m in the Neva Bay. Complex seiche level fluctuations are one of the characteristic features of the Baltic Sea regime.

Catastrophic floods are associated with fluctuations in sea level.

The Baltic Sea is covered with ice in some areas. The earliest (around the beginning of November) ice forms in the northeastern part of the Gulf of Bothnia, in small bays and off the coast. Then the shallow areas of the Gulf of Finland begin to freeze. The maximum development of the ice cover reaches in early March. By this time, motionless ice occupies the northern part of the Gulf of Bothnia, the region of the Aland skerries and the eastern part of the Gulf of Finland. Floating ice occurs in the open areas of the northeastern part of the sea.



The main problems of the Baltic Sea are related to the gradual deterioration of oxygen conditions in the deep layers of the sea, which has been observed in recent decades. In some years, oxygen disappears completely already at a depth of 150 m, where it forms hydrogen sulfide. These changes are the result of both natural changes in the environment, mainly temperature, water salinity and water exchange, and anthropogenic impact, which is expressed mainly in an increase in the supply of nutrient salts in the form of various forms of nitrogen and phosphorus.


The significance of the Baltic Sea in the national economy of the countries of the region and the ever-increasing negative impact of anthropogenic factors on the quality of the marine environment require urgent measures to be taken to guarantee the cleanliness of the sea.

Pollution enters the sea directly with sewage or from ships, diffusely through rivers or. The main mass of pollutants is brought into the sea with the flow of rivers (Neva, Vistula) both in a dissolved state and adsorbed on suspension. In addition, the seaside cities, St. Petersburg, Kronstadt, Vyborg and, to the greatest extent, the merchant and military fleets are sources of pollution of the marine environment with oil products.

The greatest harm to the marine environment is caused by toxic substances (salts of heavy metals, DDT, phenols, etc.), oil products, organic and biogenic substances. Every year, about 300 tons of oil products enter the Gulf of Finland from various sources. The main mass of nitrogenous compounds enters the sea diffusely, as well as sulfur compounds, which enter the marine environment mainly through the atmosphere. Toxic substances are discharged mainly by industry. The different nature of pollution complicates the struggle for the purity of the marine environment and requires the implementation of a complex set of water protection measures.

Monitoring of the marine environment is, first of all, the organization of systematic observations of the physicochemical and biological indicators of the marine environment at constant representative points of the reservoir.

The quality of the marine environment of the Baltic Sea generally meets the requirements of water users, but about many major cities and areas of contamination. It is alarming that over the past decades the content of toxic substances in marine living organisms has increased to two orders of magnitude, which once again indicates the need for urgent water protection measures. Great harm is caused by accidental spills of oil products from tankers. The monitoring results will make it possible to periodically check the state of the marine environment, i.e., to identify the dynamics of marine pollution.

Two small sections of the bottom of the coastal part of the Baltic Sea belonging to Russia are sharply different in terms of geoecological conditions. The most anthropogenic pressure is experienced by the inner, eastern part of the Gulf of Finland within the Leningrad region. The main area of ​​pollution was that part of the bay, which is located east of Kotlin Island, between it and the Neva delta. This happened several years ago after the construction of a dam running from Kotlin Island to the northern and southern mainland shores. An important element of the geoecological situation in the eastern part of the Gulf of Finland are numerous underwater quarries for the extraction of construction raw materials, mainly sand, which in the future may pose a threat to the stability of the coastal part of the bottom and coasts.



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