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Terrestrial Heat Flow in Areas of Dynamic Influence of Faults in The EGU Stephan Mueller Special Publication Series, 2, 153–160, 2002 c European Geosciences Union 2002 Terrestrial heat flow in areas of dynamic influence of faults in the Baikal rift zone S. V. Lysak and S. I. Sherman Institute of the Earth’s Crust, Siberian Branch of Russian Academy of Sciences, Lermontov Street 128, Irkutsk, 664 033, Russia Received: 5 October 2000 – Revised: 19 December 2001 – Accepted: 5 February 2002 Abstract. Terrestrial heat flow in the Baikal rift zone is irreg- ducted in exploratory drillholes ranging from 0.3 to 3–5 km ularly distributed. Its high values are associated with active in depth (0.3 to 1 km in ridges, 1 to 2.5 km in intermountain faults and areas of dynamic influence of faults. Stress pat- depressions, and 2.5 to 5 km on the Siberian microplate) and terns in these regions have been studied across and along from 0.5 to 2 km (mostly <1 km) at altitudes above sea level. major faults. Measurement sites under consideration are Precise heat flow measurements were carried out for several those located not farther than 30 km from the given fault weeks or several months (occasionally up to 5 years) after axis. Across the fault strike, heat flow values are revealed drilling had been complete. Results of hydrogeological and to decrease with distance from the fault axis. Along the fault cryological studies were also used in constructing the map strike, variations of heat flow values are within measurement (Lysak, 1978; 1984; 1995). errors, with the exception of thermal spring sites. It is estab- Marine studies at transversal profiles across Lake Baikal lished that heat flow values are regularly changeable. Similar were carried out by oceanographic techniques from aboard of relationships are obtained for heat flow patterns in other con- a scientific vessel. Either a thermal gradiometer (Duchkov et tinental rift zones. al., 1987) or a cable thermistor probe penetrating through 1 m to 3 m thickness of bottom sediments were used (Golubev, 1982; Golubev et al., 1993). 1 Introduction An average heat flow value of Lake Baikal basin is 78±36 mW/m2. In other rift depressions (Tunka, Barguzin), Heat flow acting from the Earth’s interiors is one of the pri- it is 62±13 mW/m2. Thermal waters of these intermoun- mary factors determining geodynamic activity of geological tain artesian basins are distinguished in the thermal field structures and activity of faults. We discuss quantitative rela- as regional anomalies. Their local high values exceed 80– tionships between heat flow values and their variations across 100 mW/m2 in the fault zones bordering these depressions. and along fault zones using data from the Baikal rift zone At the north-eastern flank of the BRZ, heat flow drops down (BRZ) and the territory of the Siberian and Transbaikalian to 50 mW/m2 and below; it can reach 70–80 mW/m2 only at microplates (Fig. 1) in the eastern part of the Eurasian con- some local fault sections (see Fig. 2). The regional heat flow tinent. The variability of these values is calculated as sums of ridges bordering the rift depressions is 40±6 mW/m2. of squares of deviations from the overall average values and An average regional heat flow of the Transbaikalian mi- double estimation error (2σ); average values of heat flow and croplate is 52±11 mW/m2. In the southern Siberian mi- density of the faults are obtained. croplate, an average heat flow value is around 38±8 mW/m2. Heat flow stations are primarily concentrated in the cen- Low values are observed at the marginal uplifts (Lysak, tral part of the Baikal rift zone (BRZ), especially within and 1988). around Lake Baikal as well as in some other southern regions Faults in the BRZ are numerous. A fault map of Fig. 3 of the Siberian microplate (Fig. 2). The database of the given shows fault directions, genetic types and ages (Sherman et heat-flow map includes data received from the on-land area al., 1992). In the BRZ central part, the 60◦ trending faults and within the Lake Baikal, from geothermal surveys con- dominate; they follow the general strike of the rift zone. Correspondence to: S. I. Sherman The north-west-trending faults are observed perpendicular ([email protected]) to the rift zone strike. In the BRZ south-western part, sub- Sibe 154 S. V. Lysak and S. I. Sherman: Terrestrial heat flow in areas of dynamic influence of faults (E rian U m R ic M A ro S pl A Angara IA at I N N P e E a S LA m st A T Da Y Da Y rh -S E ic A at a ) de r y N Lena pr o a ess p n ion la n F e A U Uppe r -A L Depr ngar T essio a Kh n ubs T T unk B Kh unk ugu a d L ang a fa l la epr dep aun M U Y al F ult ke essi A ress t A - C H aul on L ion A R t I K A F A K E B A A U L T Bar Dep guz Selenga res in B A I K A L - C H Ch sion A R A F A U L T Mu ara Dep Tokk ya de dep pre res o Vitim res ssio sion sion Tra n ns (A ba M ik O al U ian R P m L icro AT plat 2 , accordingly). E) e 2 . In intermountain2 , accordingly. de- however, these high values were not taken into consideration when the average heat± flow18 mW/m value was± estimated.3 mW/m 9 mW/m In deep bottom depressions and at underwater± uplifts and ◦ trend- blocks,±23 an and average 65 heat flow value± is9 and by 1.5 47 times lower (69 At the Transbaikalian microplate, an average heat flow value of fault zones is 71 pressions and at ridges and uplifts, average heat flow val- Block-scheme the Baikal rift zone formation. Scale 1:5 000 000 (Sherman and Levi, 1977,ues with of additions). fault zones are 52 Even in the southern part of the Siberian microplate, heat Fig. 1. flow in fault zones is higher than that in the adjacent areas. The above regularity is typical of other rift zones, such latitudinal and latitudinal faults are predominant. Transcur- as the Basin-and-Range Province, the Rio Grande rift, the rent or meridional faults are less abundant. The 45 Rhine and Rhone rifts, the East African rift system and sur- rounding areas (Table 1). ing faults predominate in the north-eastern part of the BRZ. Thus, high values of terrestrial heat flow are more charac- Their trends do not coincide with the general rift zone strike. Latitudinal faults are second in number, whereas longitudinal teristic of fault zones and, especially, of zones of active faults ones are even rarer. in rift depressions, rather than of the surrounding areas. The BRZ central part is characterized by a maximum num- is a number of faults, n within an area f ber of the Cenozoic faults trending in agreement with the BRZ general strike. At the BRZ flanks, the predominant fault 3 Heat flow and density2 . It is of calculated faults from field data and informa- trend coincides with the strike of the most extensive deep- 3 km ×10 seated faults of the basement; these faults are pre-Cenozoic 2 . Density∼5 of faults, d in age (Sherman et al., 1992; Levi and Sherman, 1995). of A non-uniform distribution of faults and heat flow values tion from geological maps (Sherman et al., 1992). A map of ±10 mW/m is evident in the BRZ and its adjacent territory. Nonetheless, density of faults in the Baikal rift zone is shown in Fig. 3b. some quantitative relationships between faults and heat flow can be revealed. 2 Distribution of heat flow in fault zones 2 . In fault zones,2 . Extremely it reaches high 87 values of heat flow Numerous active faults are revealed2 are at associated the bottom with of Lake submarine hy- Baikal±36 (Fig. mW/m 4). An average heat flow value of this area is 78 There are local sites where the submarine heat flow ex- ceeds 200–1000 mW/m over 6000–8000 mW/m drothermal vents in active fault zones (Golubev et al., 1993); o 54 o 50 un g o Ar 58 . r R o r u in la I N A N I 0 im 8 a z 30 D a . 90 L G R R a m k en le C H H C ul O er K . 0 o 7 0 R o 6 a 115 ilk 120 Sh 50 40 . 30 R . R a ra h 60 c r 50 e N ha A C BALEI . n R n R r r la a . K Ono G O L I L O G R a . g n R re im a it . K V R. R S. V. Lysak and S. I. Sherman: Terrestrial heat flow in areas of dynamic influence of faults 155 a ip s T . M O N N O M R t t lo Uldza a m R. 40 A o 50 CHITA Vitim 116 . 50 R BAGDARIN o a R U S S I A I S S U R d o 60 0 0 g . 112 R 5 5 50 In a r ly y . B 50 R a ROMANOVKA a r uy y K 70 50 .
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