gtcrustГеодинамика и тектонофизикаGeodynamics & Tectonophysics2078-502XInstitute of the Earth's crust of the Russian Academy of Sciences, Siberian Branch10.5800/GT-2019-10-2-0413gtcrust-840Research ArticleПАЛЕОГЕОДИНАМИКАPALEOGEODYNAMICSЭКСПЕРИМЕНТАЛЬНОЕ И ТЕОРЕТИЧЕСКОЕ МОДЕЛИРОВАНИЕ АЛМАЗОНОСНЫХ ПЛЮМОВEXPERIMENTAL AND THEORETICAL MODELING OF DIAMONDIFEROUS PLUMESКирдяшкинА. Г.KirdyashkinA. G.

Анатолий Григорьевич Кирдяшкин - доктор технических наук, ведущий научный сотрудник

630090, Новосибирск, пр. Академика Коптюга, 3

Anatoly G. Kirdyashkin - Doctor of Technical Sciences, Lead Researcher

3 Academician Koptyug ave., Novosibirsk 630090

agk@igm.nsc.ruКирдяшкинА. А.KirdyashkinA. A.

Алексей Анатольевич Кирдяшкин - доктор геолого-минералогических наук, профессор РАН, заведующий лабораторией Институт геологии и минералогии им. В.С. Соболева СО РАН

630090, Новосибирск, пр. Академика Коптюга, 3,

630090, Новосибирск, ул. Пирогова, 2

Alexei A. Kirdyashkin - Doctor of Geology and Mineralogy, Professor of RAS, Head of Laboratory

3 Academician Koptyug ave., Novosibirsk 630090, 

2 Pirogov street, Novosibirsk 630090

aak@igm.nsc.ruДистановВ. Э.DistanovV. Е.

Валерий Элимирович Дистанов - кандидат геолого-минералогических наук, старший научный сотрудник

630090, Новосибирск, пр. Академика Коптюга, 3

Valery E. Distanov - Candidate of Geology and Mineralogy, Senior Researcher

3 Academician Koptyug ave., Novosibirsk 630090

dist@igm.nsc.ruГладковИ. Н.GladkovI. N.

Игорь Николаевич Гладков – научный сотрудник

630090, Новосибирск, пр. Академика Коптюга, 3

Igor N. Gladkov - Researcher

3 Academician Koptyug ave., Novosibirsk 630090

kir@igm.nsc.ruИнститут геологии и минералогии им. В.С. Соболева СО РАНРоссияV.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RASRussian FederationИнститут геологии и минералогии им. В.С. Соболева СО РАН; Новосибирский национальный исследовательский государственный университетРоссияV.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of RAS; Novosibirsk State UniversityRussian Federation201922062019102247263Copyright © Кирдяшкин А.Г., Кирдяшкин А.А., Дистанов В.Э., Гладков И.Н., 20192019Кирдяшкин А.Г., Кирдяшкин А.А., Дистанов В.Э., Гладков И.Н.Kirdyashkin A.G., Kirdyashkin A.A., Distanov V.Е., Gladkov I.N.Данная работа распространяется под лицензией Creative Commons Attribution 4.0.This work is licensed under a Creative Commons Attribution 4.0 License.https://www.gt-crust.ru/jour/article/view/840

Рассматриваются термохимические мантийные плюмы, имеющие тепловую мощность 1.6·1010 Вт<N<2.7·1010 Вт и относительную тепловую мощность 1.15<Ka<1.9. Такие плюмы мы называем плюмами промежуточной тепловой мощности. Они формируются на границе ядро – мантия под кратонами в отсутствие горизонтальных свободно‐конвективных течений в мантии под ними или при наличии слабых горизонтальных мантийных течений. На основе данных лабораторного и теоретического моделирования представлена схема конвективных течений в канале плюма промежуточной тепловой мощности. Плюм поднимается (выплавляется) от границы ядро – мантия до критического уровня xкр, с которого расплав из канала плюма по каналу излияния прорывается на поверхность. Канал излияния образуется под действием силы сверхлитостатического давления на кровлю поднимающегося плюма. При уменьшении высоты массива над кровлей плюма до критического значения xкр касательное напряжение на боковой поверхности массива достигает критической величины (предела прочности) τкр. Вследствие разрушения пород массива образуется канал излияния высотой xкр, по которому расплав из канала плюма прорывается на поверхность. Представлены оценки высоты канала излияния и времени подъема плюма до критического уровня xкр. Определен объем излившегося расплава для его кинематической вязкости =0.5–2.0 м2/с. С использованием объема излияния получена зависимость глубины x, с которой расплав выносится на поверхность, от диаметра канала плюма для указанных значений . В том случае, когда x больше 150 км, расплав из канала плюма может транспортировать алмазы на поверхность. Таким образом, плюмы промежуточной тепловой мощности являются алмазоносными. На основе лабораторного моделирования определена структура течения в области сопряжения канала плюма и канала излияния для алмазоносных плюмов. Сделаны фотографии картин течения и измерены профили скорости вдоль линий тока в основном цилиндрическом канале (канале плюма) и в области сопряжения основного канала с каналом истечения. Обнаружена застойная зона, находящаяся в области сопряжения стенки канала плюма и торца, моделирующего кровлю плюма. Течение расплава в канале прорыва проанализировано как турбулентное течение в прямом цилиндрическом канале диаметром dк. Результаты экспериментального моделирования и теоретического анализа показывают, что сверхлитостатическое давление в канале плюма равно сумме напора, расходуемого на преодоление трения расплава о стенки канала излияния, и напора, расходуемого на увеличение динамического давления в нем. Получено соотношение, связывающее скорость течения расплава в канале излияния и сверхлитостатическое давление у кровли плюма.

We consider thermochemical mantle plumes with thermal power 1.6·1010 W<N<2.7·1010 W (relative thermal power 1.15<Ka<1.9) as plumes with an intermediate thermal power. Such plumes are formed at the core–mantle boundary beneath cratons in the absence of horizontal free‐convection mantle flows beneath them, or in the presence of weak horizontal mantle flows. A proposed scheme of convection flows in the conduit of a plume with an intermediate thermal power is based on laboratory and theoretical modeling data. A plume ascends (melts out) from the coremantle boundary to critical depth xкр from which magma erupts on the Earth’s surface. The magmatic melt erupts from the plume conduit onto the surface through the eruption conduit. The latter forms under the effect of superlithostatic pressure on the plume roof. While the thickness of the block above the plume roof decreases to a critical value xкр, the shear stress on its cylindrical surface reaches a critical value (strength limit) τкр.Rock fails in the vicinity of the cylindrical block and, as a consequence, the eruption conduit is formed. We estimate the height of the eruption conduit and the time for the plume to ascent to the critical depth xкр. The volume of erupted melt is estimated for kinematic viscosity of melt =0.5–2 м2/с. The depth Δx from which the melt is transported to the surface is determined. Using the eruption volume, we obtain a relationship between the depth Δx and the plume conduit diameter for the above‐mentioned kinematic viscosities. In the case that the depth Δx is larger than 150 km, the melt from the plume conduit can transport diamonds to the Earth’s surface. Thus, the plumes with an intermediate thermal power are diamondiferous. The melt flow structure at the plume conduit/eruption conduit interface is determined on the basis of the laboratory modeling data. The photographs of the simulated flow were obtained. The flow line velocities were measured in the main cylindrical conduit (plume conduit) and at the main conduit/eruption conduit interface. A stagnant area is detected in the 'conduit wall/plume roof’ interface zone. The melt flow in the eruption conduit was analyzed as a turbulent flow in the straight cylindrical conduit with diameter dк. According to the experimental modeling and theoretical data, the superlithostatic pressure in the plume conduit is the sum of the frictional pressure drop and the increasing dynamic pressure in the eruption conduit. A relationship between the melt flow velocity in the eruption conduit and superlithostatic pressure has been derived.

термохимический плюмтепловая мощностьсвободно‐конвективные течениярасплавсверхлитостатическое давлениескорость теченияканал излиянияthermochemical plumethermal powerfree‐convection flowsmeltsuperlithostatic pressureflow velocityeruption conduitРабота выполнена по государственному заданию ИГМ СО РАН. Финансирующая организация: Министерство науки и высшего образования Российской Федерации.ReferencesAtikinson E., Pryde R., 2006. Seismic Investigation of Selected Kimberlite Pipes in the Buffalo Head Hills Kimberlite Field, North-Central Alberta. Alberta Energy and Utilities Board, EUB/AGS Special Report 079, 5 p.Atikinson E., Pryde R., 2006. Seismic Investigation of Selected Kimberlite Pipes in the Buffalo Head Hills Kimberlite Field, North-Central Alberta. Alberta Energy and Utilities Board, EUB/AGS Special Report 079, 5 p.Ажгирей Г.Д. Структурная геология. М.: Изд-во МГУ, 1956. 492 с..Azhgirey G.D., 1956. Structural Geology. Moscow State University Publishing House, Moscow, 492 p. 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The authors declare that there are no conflicts of interest present.