Method of Heat Flow Mapping of Mountain-Flat Region on the Basis of Zonality of Physical Geography

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1 Proceedings World Geothermal Congress Antalya, Turkey, 4-9 April 005 Method of Heat Flow Mapping of Mountain-Flat Region on the Basis of Zonality of Physical Geography Andrey M.Boykov Russia, , Makchatchkala, Imam Schamil prospect, 39a, Institute of Geothermal Problems of Daghestan SC of RAS Keywords: heat flow, geothermal map, physical geography, zonality, correlation, map method. ABSTRACT The offered method is based on statistically significant variability of heat flow depending on the leading geologicgeographical factors. The method uses correlation of heat flow with these factors with a genetic type and the age of geological environment, with lithology, with relief, with types of soils and landscapes, with a hydrographic network and degree of soil salinity. Maps of heat flow, constructed on the basis of this method, will help to solve a wide circle of problems: location of geothermal resources, search for hydrocarbon deposits, to increase informative geological interpretations; ; and others. The technique includes consecutive performance of several stages according to five accepted methodological principles: ) interpreting the major factors of influence of geologic-geographical environment on a heat field of region; ) definition of statistical averages of heat flows and correlation-regression of connections of a heat flow with a relief in areas of homogeneous geographical zones, which characterize major factors of influence; 3) drawing up a complete set of intermediate working maps constructed on the basis of mosaic mapping of region by areas with identical values of heat flow, which characterize the basic geologic-geographical factors of influence; 4) imposing against each other of intermediate working maps and estimation of reliability of drawing of configurations of heat flow isolines on a final map of geothermal field of region; 5) construction of the final map of the heat flow isolines for the region as a regional standard of background variability of heat flows near the surface. The method is illustrated by means on the example of the map of the heat flow of Daghestan (Northern Caucasus, Russia) in scale : with the isolines at an interval of 5 mw/m.. INTRODUCTION The study of regional variability of field of heat flow of the Earth is an urgent task for fundamental and applied science. The interest in the first case represents variability of average values of heat flow near the surface depending on the leading geology-geographical factors, and also correlative interrelations of heat flow with these factors (geomorphology stratigraphy and lithology of rocks, types of soils, landscape, hydrographic network, soil salting degree etc.). The new knowledge received as a result of such researches, can be used for solving various problems in sciences about the Earth. The study of variability of regional background of heat flows at surface is urgent and in the second case, for example, for geological interpretation of thermal survey. Information value of these surveys considerably grows, if it is known how various kinds of physical geographic zonality are quantitatively shown in the field of heat flows. Genesis of anomalies of an infrared survey of the surface cannot be often identified for sure. If there are no maps of background regional variability of geothermal field, it is impossible to proceed from qualitative to quantitative interpretation of such anomalies; in particular, it is impossible to solve a reverse problem of geological prospecting. In this report the new methodology is described which allows carrying out mapping of background regional variability of heat flows in regions with diverse variability of geologic-geographical environment. The substantiation of methodology is given by the example of mapping of geothermal field on the territory of Daghestan Republic (Northern Caucasus, Russia).. STATEMENT OF THE PROBLEM The methodology includes consecutive performance of several research stages according to five methodological principles: ) revealing of key factors of influence of geologic-geographical environment on the region geothermal field; ) comparative characteristics of these factors on the basis of statistical average heat flow and correlative regressive dependences of heat flow relief in homogeneous geographical zones; 3) drawing up a complete set of intermediate working maps on the basis of physical geography mapping areas with identical values of heat flow, which are characteristic for the leading geologicgeographical factors of influence on the geothermal field in view of regional variability of relief; 4) imposing intermediate working maps on each other, overlapping and estimating reliability of isolines con figurations and heat flow anomalous to draw up the final region heat flows map; 5) constructing the final map of region heat flows isolines as the regional standard of background variability of geothermal field at the surface. The problem was carried out on the basis of library and field studies, including approximately 00 measurements of heat flow determined in boreholes within the range of depths from several tens up to the first hundreds meters. The determinations of heat flow in boreholes were carried out by the different authors, but using the standard technique on the basis of geothermal gradient and heat conductivity of rocks. Data coverage is not uniform. Geologic-geothermal section of plain and foothills is well investigated, but mountain regions where there are no deep prospecting boreholes, are poorly investigated. It is impossible to consider accuracy of temperature changes in the boreholes above 0. 0 C, of heat conductivity higher than 8%, of heat flow higher than 5%.

2 3. KEY FACTORS OF GEOLOGY-GEOGRAPHICAL ENVIRONMENT INFLUENCE ON GEOTHERMAL FIELD OF REGION Key factors of influence of geologic-geographical environment on the geothermal field of the region. Previously we shall estimate the role of prospective factors of influence. In particular, relief and landscape, as it is know, are well shown on space snapshots of the terrestrial surface. Both there factors are closely connected. The analysis of the complete set of maps, which are included in the geographical atlas of Daghestan (Atlas of Daghestan Republic, 999), shows that the geomorphologic map correlates with the map of landscapes in the most degree. But genesis of landscape is secondary in relation to the relief. Therefore we shall accept as a working hypothesis, that in relation to space snapshots of the surface the leading factor of influence of geologic-geographical environment on the of heat flow is relief. At the same time, types of relief, soils and vegetative associations determine variability of landscapes in relation to soils and vegetation, which are composed under influence of climate and features of relief. All these natural factors and components of geographical environment are in close interrelation and, hence, influence formation of geothermal field at the surface. But heat flow from the interior of the Earth to the surface is determined in the holes on the basis of measurements of geothermal gradient (g) and heat conduction of rocks (λ) by the design formula: q = gλ. All these parameters depend on variability of geological environment, first of all its stratigraphy and lithology. And both these factors are in their turn interconnected with variability of relief. Landscape as a component of geologic-geographical environment is supervised by the relief as the leading geological and geographical factors of influence. The area of researches (territory of Republic of Daghestan) differs in sublatitude and submeridian directions by sharp geomorphological variability: from mountain ranges through foothills up to seaside plain of the Caspian Sea. Various kinds of zonality of physical geography parameters are observed at the background of variability of relief, what gives an opportunity to compare them with variability of heat flow field of the region. q, mw/sq.m , 84,3 30,9 56,5 78,9 59,5 70,9 55,9 76, Numbers of histograms Figure. Average values of heat flow compared to lithology near the surface. Histograms -9 are modern deposits (Q3, Q4), sandy-clays (Ak+Ap), limestones (Sm3), clays (Sm+), sandy-clays (Kn+Kg, Č+t), clays (Pg3), carbonate (Pg+, Pg3), limestones (K), clays clays (K, K and J, J). Therefore mentioned above key factors of influence of geologic-geographical environment on the region heat field must be characterized quantitatively. Such analysis is possible on the basis of statistical average of flows for homogeneous geographical zones, and also stratigraphic and lithologic complexes of rocks rising to the surface and definition of correlative-regressive dependences of variability of heat flows on relief with their limits. q, mw/sq.m , ,3 30,9 56,5 97,7 85,4 85, 70,9 59,5 55,9 47, Numbers of histograms Figure. Average values of heat flow in stratigraphic complexes near the surface. Histograms - are Chvalinsky layer, Akchagil-Apsheronsky layer, upper Sarmat, middle and lower Sarmat, Konksko-Karagansky layer, Chokrak- Tarchansky layer, Maikop, upper, middle and lower Palaeocene, upper Chalk, lower Chalk, middle Jurassic, lower Jurassic. 3.. Lithology and Stratigraphy We make type-design of average values of heat flows for the investigated territory. In particular, the intervals of maximal, minimal and intermediate values of heat flows, characteristic for lithological complexes and stratigraphic horizons, rising to the surface are determined by us with this framework. This framework can serve as an authentic geologygeographical characteristic of variability of the region geothermal field. Histograms of variability of heat flows, which are given in figures and, include the following intervals of values Lithological Correlations of Heat Flows It includes: ) maximal values of heat flow (within the interval mw/m ), describing complexes of sandyclay sediments; ) minimal values within the interval mw/m, describing upper Sarmat lime-stones and modern sediments; 3) intermediate values, describing carbonate sediments (70.9 mw/m ) and middle Sarmat clay complex (56.5 mw/m ) Stratigraphical Correlations of Heat Flows It contains: ) maximal values of heat flow within the interval mw/m, describing Konksko-Karagansky, Aktchagilsky-Apsheronsky, low Cretaceous and middle Jurassic stratigraphical horizons; ) minimal values within the interval mw/m, describing upper Sarmat and Chvalinsky horizons; 3) intermediate values, describing top, middle, low Paleocene (70.9 mw/m ) and Maikop series (59.5mW/m ).

3 q, mw/sq.m , ,7 6, 66,3 47, 48,7 48 5,8 48,9 Foothill and Inside Mountain Daghestan, where areas of meadow and wood vegetation are represented, that for areas of plain meadows and also flux and desert vegetation ( mw/m ) in Plain Daghestan. Thus some correlation with relief is observed here, what will find its reflection while imposing intermediate working maps of heat flow against each other Numbers of histograms Figure 3. Average values of heat flow through soils. Histograms -0 are light-chestnut saline soils, alluvial-meadow soils, meadow-chestnut saline soils, sands, saline lands, meadow saline soils, meadow-chestnut soils, meadow-carbonate soils, brown soils, mountain-meadow soils. 3.. Soils Average values of heat flow, as it follows from figure 3, in homogeneous soils areas break up to two intervals: a) the highest values of heat flows group in the interval mw/m, and low values within the interval mw/m. Mountain-meadow soils with their high average value of heat flow (66.3 mw/m ) occupy considerable territories in Mountain Daghestan. But in the whole precise division according the values of heat flow is not characteristic for soils, of plan and mountain territories. If is explained by the fact that soils of plain territories are represented widely enough in the Mountain Daghestan, though specific mountain types of soils are absent on plain. The values of heat flows on the map of soil areas, as this implies, can correlate with relief in the Mountain Daghestan not everywhere while imposing intermediate working maps against each other, but they can on the considerable part of this territory. This concerns, accordingly, the values of heat flows received by means of correlative-regressive analysis. q, mw/sq.m ,9 46,4 39,8 39,5 5,9 66,6 67, 65, Numbers of histograms 38,3 Figure 4. Average values of heat flow in areas of vegetable associations. Histograms -9 are grass, rush, grass and rush, bushes, trees, bushes and trees, meadows, meadows and trees, sands. 3.3 Vegetation Vegetation is represented on the greater part of the Mountain Daghestan by Alpine and Subalpine meadows. But these areas are not covered with drilling and, accordingly, there are no definitions of heat flows for areas of their landscapes. Therefore, connections between values of heat flows and vegetation were studied in our analysis mainly for the Plain Daghestan and intermediate plainmountain territories. The higher interval of values of heat flows ( mw/m ) is more characteristic, as it is seen from the diagram of average values of heat flows in areas with homogeneous vegetation on the figure 4, for 3.4. Soil Salinization Degree Analysis of interrelations of heat flows with areas of soil salinization has essential importance, as it increases the number of taken into account factors of influence of geographical environment on the field of heat flows. It raises reliability of mapping. Areas of salinization are connected closely enough with relief: they are absent in Foothill and Mountain Daghestan, but cover the main part of territory of Plain and Seaside Daghestan. Thus areas of salinization on plain, which is important for our analysis, are located not only in the basins of numerous rivers to the north of Daghestan wedge, but also in droughty half-desert and desert zones in the north. It corresponds with geomorphologic zoning within Terek-Sulak delta-alluvialsea plain and on the territory Terek-Kuma accumulativealluvial sea Chvalinsky plain. There fore the scope of flat territories by the intermediate working map of heat flow will be rather representative. q, mw/sq.m ,3 49, Numbers of histograms Figure 5. Average heat flows in areas of salinization (salinization degree in % from agricultural areas). Histograms -4 are saline soils (0.8%), strong salinization ( %), middle salinization (0. 0.4%), weak salinization (0. 0.%). The values of average heat flows, as it is seen from the diagram on the figure 5, are grouped not according to the degree of increasing or decreasing percentage of salt in soil. They are close on histograms, 3, 4. But the area of strong salinization ( %) with low value of average value of flow on histogram serves a kind of a buffer zone between high values of heat flow within the interval mw/m, characteristic for the rest of areas of salinization. However the nature of this geothermal buffer is not clear yet Hydrographic Network Hydrographic factor can influence near surface heat field directly only totally on condition that there is rich enough hydrographic network. Thus, strong, but indirect influence of other factors is possible. Hydrographic manifestations certainly, do not influence directly measured heat flows, their influence is indirect and weak. It concerns dot or local surface self-issued sources and reservoirs. The degree of influence of hydrographic factor depends on a combination of other geologic-geographical factors, including hydrogeological one. The histogram given on figure 6 confirms it. The high values of heat flows ( mw/m ) as it follows from figure 6, are located in the basins of rivers and 3

4 near irrigation channels. But bottom land flood basin of the rivers are usually located in linear zones of down turn of relief, as the rivers on plan lay the way, as a rule, along lines of healed faults rising up the surface. It is known from classical geotectonic , ,5 q, mw/sq.m ,3 43, 40, Numbers of histograms Figure 6. Average values of heat flows in hydrographic network. Histograms -4 are channels, rivers, reservoirs, springs, artesian wells. Channels, being artificial hydro-engineering structures, are also frequently projected along natural downturn of relief. Therefore, treys, in the same way indirectly reflect a fault network. As heat flows are mostly allocated in fault zones with higher values, it is reflected in statistical parameters of heat flows, determined near the elements of a hydrographic network. The influence of the hydrographic factor on the values of heat flows is shown, thus, indirectly, through relief and fault tectonics. 4. CORRELATION CONNECTIONS, CAN CORRELATE HEAT FLOW WITH RELIEF Heat flow, as it is known, can correlate both with underground relief and surface relief. We shall examine mainly, interrelations of heat flow with surface relief with the limits of homogeneous geographical zones. Therefore, we shall illustrate only on one-example connections of heat flows with underground relief within the region, by specifying the area of practical use of correlation dependence. The illustrate this correlation we can use two geology-geothermal sections, constructed according profiles, oriented from north to south, location of which is shown on the scheme of figure 7. The profile curves of heat flows, as it is seen from the sections given on figures 8 and 9, repeat approximately, with different degree of accuracy, contours of foot or roof of stratigraphic horizons along the sections and appreciably surface relief. Thus the values of heat flows in each point are determined, that is necessary to mean, naturally, not only by surface relief or underground relief, but by influence of other factors as well. The influence of outcrops to the surface at the points of watch of different lithologic-stratigraphical complexes with different heat conduction can be attributed, in this case, to these factors. Figure 7. Daghestan Republic (Russia) map with profiles of heat flows:, are profile, profile. The influence of faults also effects, if their location coincide with the points of determinations of heat flows. It is necessary to note on the whole, that the factor of relief in conditions of mountain-flat zone, influences directly or indirectly primarily the formation of a regional geothermal field. We have established on the basis of comparison of heat flow values, determined within the interval m, existence of correlation with underground relief. Correlation dependence was established between profile curves of heat flow (q, mw/m ) and underground relief of regional water confining layer on depth of the roof of Maikop sediments (H, m). The correlation is a kind of nonlinear regression with a standard deviation S equal 8 mw/m : q = / H () If is possible to consider accuracy of definition of regional heat flow on the basis of this equation of regression quite satisfactory for forecast estimations. The geothermal background can be estimated by the data of bedding of Maikop sediments roof (N Pg 3 ) on the territory of the region not covered by geothermal watch. The received data can be used while modeling geothermal fields and designing technical geothermal objects. The fact of correlation of heat flows with the relief of the roof of regional water confining layer Maikop clays indicates insignificant regional influence of fluid convection in the upper hydro-geological floor on the heat flow field. It follows that, regional base heat power potential of the investigated region is determined by geothermal features of geological section from the depth below the roof of Maikop stratigraphic horizon. 4

5 Figure 8. Geological section and heat flow curve on profile. Figure 9. Geological section and heat flow curve on profile. 4.. Correlation of Heat Flow with Relief We carried out correlative-regressive analysis for values of heat flow both in areas of homogeneous geographical zones and for the whole territory of the region. The results of the analysis are given in table. As one can see from the table all regressions, connecting heat flow values with the relief for all areas taken for analysis are in this case linear. On the background of general domination of straight regressions, two, dated to the areas of trees, are represented by reverse regressions. In view of rather small values of standard deviations (S reg ) from the lines of regression, which serve in correlative-regressive analysis as parameters of accuracy of heat flow definitions on regression equations, all dependences can be used for practical calculations of heat flow values by absolute marks of day time relief in the regions which are not covered by boreholes and for which definitions of heat flow are absent Manifestation of Self-Similarity in the Field of Heat Flows of Geographical Environment The abovementioned diagrams of heat flows allow to make a general conclusion that average values of heat flows are arrange for homogeneous areas of landscape. They are statistically expressed, but no so clearly, as average, values of heat flows characteristic for stratigraphic and lithologic complexes of mountain rocks, rising to the surface. The sandy-clay complexes, as it is seen in figures -, were sharply distinguished by higher values (76+85 mw/m ), but modern deposits and Sarmat limestone s by lower values (30+40 mw/m ). Difference of values of heat flow between these intervals is approximately 45 mw/m. The 5

6 intermediate position (55+7 mw/m ) was occupied by clay, upper Cretaceous limestone s and Carbonates of Paleocene deposits. Equally significant differences of heat flows average values between landscape areas are absent. As it can be seen, for example, from figure 4, they reach no more than 9 mw/m. It means, that statistical variety of clearly marked landscapes in geothermal field is smoothed out by influence of a factor of through action. Landscapes, apparently, are formed simultaneously under control of this factor. The surface relief is, obviously, such a factor within the framework of the working hypothesis accepted by us. The required factor of through action can be identified on the basis of study of kinds of influence of surface relief on geographical environment. They are shown in the character of steady interrelation of components of landscape and geothermal field. The study of relation of statistical heat flow values on the territories of Mountain, Foothill and Flat Daghestan with stratigraphic and lithologic complexes, and also with kinds of geographical zonality, complemented by correlativeregressive analysis of interrelations of heat flow with relief on the regional and local levels made it possible to establish one-parametrical self-similarity of the field of heat flow of geographical environment through controlling factor of relief. It substantiates in the future principal opportunity of using concept of fractals for the study of geologygeographical environment on the basis of representation of the whole hierarchical line from regional up to local as fractal sets. The analytical opportunities of this concept are realized through use of solutions of differential equations in fractional derivatives, in particular heat conduction equations (Maylanov, 000), which considerably raises, for example, information of analysis of abnormal manifestations of seismogeneous and other nonlinear geodynamic processes in geothermal field (Boykov, and Maylanov, and Magomedova, 00). System of proofs and substantiation of property of geographical environment self-similarity are deduced by analogy with property, known in physics, as mechanical similarity of dependence of potential energy (u ) on distance ( r ), which is given in (Landau, and Livshiz, 973): k u ar, ar,..., ar ) = a u( r, r,..., r ), () ( n n where a is any constant, and k is degree of uniformity of function. After transformations we come to relation r a ar a Thus potential energy the system is homogeneous function k degree of coordinates. Then equations of movement assume vectorially similar trajectories. That is, changing all coordinates of particles in identical number of times means transition from one kind of trajectories to another, vectorially similar to the first ones and distinguished from them only by linear sizes. From here by analogy the property of one-parametrical selfsimilarity of geology-geographical environment can be expressed on the basis of correlative-regressive dependence of energy characteristic heat flow (g) on height of relief (h) in landscape zones by relation: g ( h k a h) ± S ( a h) = a [ g ( h) ± S ( )], (3) where h a h a. Here h = h h, S is a height relief, difference within the limits of area or homogeneous 6 landscape zone, standard deviation from regression diagram. Sealing of geology-geographical environment on the example of calculation of constant self-similarity a is characterized in the data of table where landscapes are represented by hierarchy of three ranges (regional, intermediate which contains internal hierarchy of two ranges, and local). The obvious objective law follows from the table: ) in landscape areas, covering mountain-flat transitive zone (North Daghestan and Mountain Daghestan areas), there is constant self-similarity a > 0 moreover, a 0, ) in landscape zones of the low flat zone (North Daghestan area) a < 0 and it varies within large limits: This objective law testifies to higher regulation of selfsimilarity in the transitive mountain-flat zone that is in flat zone. Geothermal aspects of objective law can be characterized on the same date basis. The standard deviation (S) from average value of heat flow (q avge ) we shall compare for this purpose with standard deviations (S reg ) of values of heat flow q from histograms of heat flow regressions and height of relief, and also with constants self-similarity a, which are given in table 3. The data from the table show, that within general area of all kinds of landscape, relief ( level of hierarchy, mountainflat transitive zone is one of the possible factors influencing heat flow value, as S =.6 S reg =.5. Maximum deviation of value q avge in landscape zones -3 levels of hierarchy from value q avge of general area of all components of landscape ( level of hierarchy) makes only 8.3%. However, it a little bit higher and reaches.3% inside the general area of salinization in relation to more homogeneous landscape zones of salinization. Relief is the a major factor influencing variability of heat flow within landscape zones -3 levels of hierarchy, as S reg in them is almost always less, than S. Exception is the landscape zone of rush and grass ( level of hierarchy), where S and S reg are equal at the constant self-similarity, maximal on absolute value (a = -3.4). Here, relief is one of the probable factors of influence. But absolute value of parameter of self-similarity in this case is not a significant factor as in the zone of strong and very strong salinization (3 level of hierarchy), with S S reg = 9.0 it is expressed by the value (a = -.), close to the minimum. Thus in the whole, correlation between levels of hierarchy, degree of divergence of values S and S reg and a values is not observed. In the sense of degree of order of self-similarity the sign of value a has a priority value. The high degree of order of self-similarity of geographic environment, manifesting in geothermal field is a parameter of long-term stability of landscape (at least, in scale of historical time). This conclusion concerns mountain-flat transitive zone of Daghestan. But it is not spread on the flat zone where high degree of order of self-similarity is absent. The conclusion is coordinated with geological ideal on the whole, because mountain-flat transitive zone is on the stage of stable geological development. Hence, the intensity of orogenesis, expressing in variability of relief, will not exceed the first centimeter per one year. On the contrary in the flat North Daghestan area the influence of exogenous natural relief formatting factors can be more intensive, with will be expressed in variability of landscape (instability in scale of historical time).

7 5. THE METHODOLOGY OF CONSTRUCTING MAPS OF GEOTHERMAL FIELD FOR THE TERRITORY OF DAGHESTAN Methodology is based on gradual use of results discussed above, in cartographical purposes. The methodology doesn t envisage introduction of corrections on relief. First, influence of has been already taken into consideration in obtained statistical average values of heat flow for the mountain-flat territory. Second, heat flow is calculated by regression equations of inside zonal physical geography just by variability of relief. 5.. The Stage Making Intermediate Working Maps Heat flow maps at this stage are being made as maps of mosaic type. They are being made in the same scale with sharply expressed borders of areas of homogeneous geographical zones. All values of heat flow within such areas in any point correspond to average value of heat flow, received for the given area (see histograms). Thus, we receive a complete set of intermediate working maps, on which there is a difference of values of heat flow on borders of neighboring areas. We constructed for the territory of Daghestan five kinds of such mosaic maps of heat flow, which corresponded to stratigraphy and lithology of rocks, soils, hydrographic network, vegetation and area of salinization. 5.. The Stage of Imposing and Comparison of Maps with Estimation of Reliability of Construction of Fragments of General Final Map Degree of concurrence of average heat flow values for areas at this stage is estimated in places of imposing maps against each other in this case, in five layers, and they choose the most authentic values for units of regular grid on the map. The grid is put in scale of used working maps (from 5 5 km or more). It serves a cartographical basis for construction at the following stage of general final map of heat flow. Then use of average heat flow values as units of interpolation on grid is similar to smoothing by multiparametrical interpolation. We considered authentic in our case values of heat flow in units of interpolation, which coincided within the limits of standard deviations on four of five working maps. This technique is quite justified by rather small on the whole divergences between average values of heat flows for areas of different kinds of geographical zonality. For example, maximal deviation q avge in homogeneous geographical zones from q avge for incorporated area, including all landscape zones, has made 6.3 mw/m or 8.3%. The specific features, characteristic for operation of overlapping, were, however, revealed while imposing and comparing working maps with each other. The tendency to manifest the greatest discrepancy of for the same unit of grid in some pairs of working maps. In depended for example, on the range of heat flow average values within the limits of the histogram (see above figure -6), on which heat flow average value of this map for the given unite of grid fell. Such divergences were observed for the ranges with low and high values of heat flows. We applied calculations of heat flow values for the grid units according to correlative-regressive dependences, if divergences between the values of average heat flows on different working maps their overlapping were too great, or the number of tallying values was less, than on the four working maps. We used in this case values of absolute marks of relief for the given point, which we set in regression equations for calculation of heat flows. The heat flow values, received from the regression equation, was added together with the values, received from comparison of working maps. Arithmetic mean was given to the grid unit on the map, intended for realization of the last stageconstruction of the final map The Stage of Final Map Construction This stage is prepared by operations made at the previous stages. The advantage of our methodology consists in imposing against each other heat flow mosaic maps made on the basis of different kinds of geographical zonality. Finger-pattern mosaic of each intermediate working map makes it possible by repeated overlapping to cover and extrapolate average heat flow values of units to such areas, where homogeneous geographical zones spread, but where there are no heat flow measurements in boreholes. Thus, white spots on the heat flow map can be reduced to a minimum without essential reduction of reliability. The correct choice of heat flow isoline step on the final map is very important. The isoline step should exceed maximal absolute error of definition of heat flow value at all preparatory stages in all used operations. Simultaneously, map step should be sufficient for characteristic geologygeographical features of territory can be shown on the maps. We have chosen isoline step equal 5 mw/m while constructing the map of the regional background heat flow of Daghestan Republic. Map scale is : Heat flow isolines on the basis of interpolation of heat flow values with such step between grid units were constructed on the final map. Such step allows, without increasing heat flow map error to reveal both regional and local anomalies provided reasonable increase of density of grid). 7

8 Figure 0. Heat flows map of Daghestan Republic (Russia) with isolines in mw/m. 8

9 6. HEAT FLOW MAP OF DAGHESTAN REPUBLIC AND CARTOGRAPHICAL APPENDIX The final map of heat flows is represented in figure 0. The geological interpretation of the map is executed on the basis of the created complete set from auxiliary maps of Daghestan Republic regional geothermal field at the surface. Each map of the complete set includes geologicgeographical basis as one of kinds of scanned physicgeographical maps of Daghestan. The background regional heat flow map of Daghestan with a step 5 mw/m, made with the help of vector graphics was imposed on this basis as the second layer. This map is submitted in figure 0. The overlapping was reached with the help of joining administrative borders of Daghestan on both maps. The summary map after that was kept in one layer image. The complete set of cartographical basis is all kinds of physic-geographical maps of Daghestan territory, submitted in the geographical atlas (Atlas of Daghestan Republic, 999). These are physical, geological and tectonic maps, tectonic scheme of Mesozoic complex, map of seismic activity and seismic zoning, geoisotherm map, geomorphologic, map of orography and landscape map, map of physic-geographical zoning, soil map and map of salinization, map of vegetation. This cartographical complex covers all most essential regional manifestations of geology-geographical factors at the terrestrial surface. It has allowed for the first time to execute adequate interpretation of data of geothermal mapping in the region. 6.. Methodology of Interpretation of Heat Flow map of Daghestan The complete set from maps, submitted in present report, is intended for viewing in the window of the program CorelDraw 0. Geologic-geothermal interpretation requires strong increase of scale of maps, which enables detailed interpretation of any map of the complete set. We have made such interpretation, during which anomalies of heat flows field, characteristic for areas of various kinds of zonality of physical geography were revealed and identified. We have made on this basis the report of obvious geothermal and geographical correlates. These correlations allow carrying out interpretation of the data, both thermal space survey and other kinds of regional geothermal mapping on the authentic cartographical geologicgeographical basis. Geothermal parameters (intervals of heat flow values and average values of heat flow), taken from the background regional heat flow map in figure 0, put according their correlates as elements of structural geology, tectonics, stratigraphy, lithology, seismic zoning or areas of this or that zonality on the maps of physical geography. The report of revealed correlates is shown in the tables, which serve as a tabulated addition to the specified complete set from cartographical appendices. The appendices and tabulated additions should be considered as a single unit while interpreting data of geothermal surveys. The tabulated addition is submitted below (Table 4 -). 7. CONCLUSIONS This report contains exposition of new method of constructing heat flow maps of mountain-flat region on the basis of using zonality of physic geography. The method is illustrated on the example of constructing the map of the territory of Daghestan Republic in Russia. The method is substantiated by the following conclusions:. Lithological and stratigraphical complexes, areas of vegetative associations, areas of homogeneous soils, areas of salinization of various degree and elements of hydrographic network are shown as major factor of influence of geologic-geographical environment on the heat field of the region at the surface in the mountain-flat region.. Qualitative and quantitave estimations of these factors of influence are executed on the basis of type-design practice of statistical average values of heat flows and correlativeregressive dependences through relief, which are established for all areas of homogeneous geographical zones, in which these factors are shown. 3. Correlative-regressive connection between heat flows and relief is illustrated on the example of geological sections and variability of heat flows by two profiles. 4. The property of one-parametrical self-similarity of geologic-geographical environment is shown in the field of heat flows through relief within the limits of zonality of physical geography and can be characterized quantitatively with the help of values of self-similarity constants. 5. Technology of construction of heat flows maps on the basis of using zonalities of physical geography is developed and methodologically substantiated. 6. The new method of constructing maps of heat flow in the mountain-flat regions is illustrated with the regional map of background heat flows on the territory of the Daghestan Republic (Russia), constructed on the basis of the offered technology. 7. The heat flows maps was compared with all kinds of physic-geographical maps of Daghestan, which has shown reflection in anomalies of heat flow of various elements of physical, geological and tectonic maps, tectonic scheme of Mesozoic complex, map of seismicity and seismic zoning, geoisotherms map, geomorphologic, orographical and landscape maps, maps of physic-geographical zoning, maps of soils and salinization maps, map of vegetation. REFERENCES Atlas of Daghestan Republic. Federal service of geodesy and cartography of Russia, Moscow, 999 (in Russian). Maylanov R.P.: Concept of fractal in the theory of heat field of the Earth, submitted to The Earth s Thermal Field and Related Research Methods, Moscow (000). (In Russian). Boykov, A.M., and Maylanov, R.P., and Magomedova, E.F.: Analytical method of the fractal concept as basis of analysis of temperature regime of entrails seismic activity, Proceedings, Geodynamics and Seismicity of East Caucasus, Makchachkala (00). (In Russian). Landau, L.D., and Livshiz, E.M.: The Mechanics, Edition third, Science, Moscow, 973. (In Russian). 9

10 Geographical zone Table. Type of regression (units of measure: q, mw/m ; h, m) Incorporated area of all landscape zones q = 0.007h ±.5 Area of meadow vegetation q =0.4 h +44. ±.7 Area of trees q = -0.0 h ±8.4 Area of grass and trees q = h ±7.5 Area of hydrographic network q =0.7 h ±4.5 Incorporated area of all zones of salinization q =0.9 h +6.8 ±.6 Area of strong and very strong salinization q =0.3 h ±9. Area of average and weak salinization q =.4 h ±. Area of average salinization zone q =.74 h +8.8 ±3.0 Standard deviation from S the line of regression Levels of hierarchy of landscape Zones of physicgeographical zoning North Daghestan and Mountain Daghestan areas Table. Zones of natural components of landscape General area of all kinds of landscape Constant self-similarity α North Daghestan area Rush and grass -3.4, (α= H / h ) North Daghestan and Mountain Daghestan areas North Daghestan and Mountain Daghestan areas North Daghestan and Mountain Daghestan areas Meadow vegetation.0, (α= H / h ) Trees., (α= H / h ) Hydrographic Network., (α= H / h ) North Daghestan area General area of salinization -88.0, (α= H / h 3 ) 3 North Daghestan area 3 North Daghestan area Zone of strong and very strong salinization ( %) Zone of weak and average salinization (0. 0.4%) -., (α= H / h 3 ) -.8, (α= H / h 3 ) Table 3. Landscape Zone q avge ± S S reg. α Rush and grass 39.8 ± 7.5 ± Trees 5.9 ± 0.9 ± Meadow Vegetation 67. ± 3.4 ±.6. Hydrographic Network 55.5 ± 8. ± 4.5. General area of salinization 49.4 ± 5.4 ± Zone of strong and very strong silinization 43.8 ± 9. ± Zone of weak and average salinization 48.7 ± 4. ±. -.8 General area of all kinds of landscape 50.9 ±.6 ±.5 α = H / h, where H, h is relief height difference at levels or of hierarchy, difference at the levels or 3. 0

11 Table 4. Correlates of geothermal parameters on the geological map of Daghestan Deposits age group/ geothermal parameters Cenozoic group Upper Miocene 3 N Genetic types and age of deposits Middle Miocene N Oligocene-lower Miocene P 3 Heat flow interval, mw/m Average value, mw/m Mesozoic group Upper Chalk K Lower Chalk K Middle Jurassic J Lower Jurassic J Heat flow interval, mw/m Average value, mw/m Table 5. Correlates of geothermal parameters of heat flow on the tectonic map of Daghestan Geothermal parameters Faults Axes of main anticlines Group of buried raisings Faults marking fold slope of Terek- Caspian advanced deflection Narat-Tubinsky fault Kadar-Irganaisky anticline Mugrinsky and Gamry-Osensky breaks, marking, the ledge of the Daghestan wedge Heat flow interval, mw/m Average value, mw/m Table 6. Correlates of geothermal parameters on the map of orography of Daghestan. Geothermal parameters between Names of ranges (height ranges, m) mountain ranges Range Arakmeer range Gimrinsky ( ) Heat flow interval, mw/m Average value, mw/m 55.5 Range Arakmeer range Arzuta, range Zonogoch ( ) Heat flow interval, mw/m Average value, mw/m 55.5 Ranges, contouring the area between the villages Dilim and Dubky from the south, east, north and west (lower 000) Heat flow interval, mw/m 58 Average value, mw/m 58 Table 7. Correlates of geothermal parameters on the map of physic-geographical zoning of Daghestan. Geothermal parameters Tersko- Kumskaya flat province Foothill Daghestan Inside-mountain Daghestan High-mountain Daghestan Sea-side Daghestan province Heat flow interval, mw/m Average value, mw/m

12 Table 8. Correlates of geothermal parameters on physical map of Daghestan. Geothermal parameters Mountain rivers Flat rivers Sulak Samur Achtitchai New Terek Heat flow interval, mw/m Average value, mw/m Table 9. Correlates of geothermal parameters on the map of geoisotherm 60 0 С of Daghestan. Geothermal parameters Depths of geoisotherm 60 0 C, m Heat flow interval, mw/m Average value, mw/m Table 0. Correlates of geothermal parameters on Daghestan soils map. Geothermal parameters Soils of flat territories Marsh Sands Saline lands Heat flow interval, mw/m Average value, mw/m 40, Greyish-brown wood steppe like Dark-chestnut Greyish-brown wood Heat flow interval, mw/m Average value, mw/m Meadow-chestnut Heat flow interval, mw/m 43 Average value, mw/m 43 Soils of mountain territories Mountain-valley Heat flow interval, mw/m 58 Average value, mw/m 58 Table. Correlates of geothermal parameters on the map of seismic activity and seismic zoning of Daghestan. Geothermal parameters Epicenter zones of earthquakes By tool data By microseisms of before tool period Seismic activity and seismic zoning Zones of intensity of earthquakes in numbers on on mark scale Heat flow interval, mw/m Average value, mw/m