Subduction Style at Different Stages of Geological History of the Earth: Results of Numerical Petrological-Thermomechanical 2D Modeling

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Abstract

In this article we examine the effects of impact of slab rocks eclogitization on the subduction regime under the continent. Eclogitization of rocks in high-pressure metamorphic complexes occurs only in the areas of penetration of hydrous fluid. In the absence of hydrous fluid, the kinetic delay of eclogitization preserves low-density rocks under P‒T conditions of eclogite metamorphism, delaying the weighting of a slab and reducing the efficiency of the slab-pull mechanism which contributes to the steep subduction into the deep mantle. The results of numerical petrological-thermomechanical 2D modeling of subduction under the continent in a wide range of eclogitization parameters of oceanic crust rocks (discrete eclogitization) are presented. The effects of a lower kinetic delay of eclogitization in the water-bearing basalt layer, compared to the drier underlying gabbro layer, have been tested. Based on results of 112 numerical experiments with 7 variants of eclogitization ranges (in range 400–650°C for basalt and 400–1000°C for gabbro) at different potential mantle temperatures (ΔT = 0–250°C, above modern value), and steep, flat and transitional subduction regimes were identified. The mode of steep subduction occurs under modern conditions (ΔT = 0°C) with all ranges of eclogitization. Here it is characterised by an increase in the angle of subduction of the slab as the plate descends, and above the boundary of the mantle transition zone there is a flattening or and then tucking of the slab. Subduction is accompanied by the formation of felsic and mafic volcanics and their plutonic analogues. At elevated temperatures of the mantle (ΔT≥150°С) and discrete eclogitization over a wide range, the flat subduction regime is observed with periodic detachments of its steeper frontal eclogitized part. The flat subduction regime is accompanied by significant serpentinization of the mantle wedge and episodic, scarce magmatism (from mafic to felsic), which occurs at a significant distance (≥500 km) from the trench. During the transition regime, which is also realised in models with elevated mantle temperatures, there is a characteristic change occurs from flat to steep subduction, resulting in a stepped shape of the slab. As the kinetic shift of eclogitisation increases, flat subduction develops. An increase in the thickness of the continental lithosphere from 80 km to 150 km contributes to the implementation of steep subduction, while the influence of the convergence rate (5–10 cm/year) is ambiguous.

Discrete eclogitization of thickened oceanic crust and depletion of lithospheric mantle in the oceanic plate are the main drivers of flat subduction. In modern conditions, their influence becomes insignificant due to the decrease in the thickness of the oceanic crust and the degree of depletion of the oceanic mantle lithosphere. As a result, the less frequent flat movement of slabs is determined by other factors.

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About the authors

V. S. Zakharov

Lomonosov Moscow State University

Author for correspondence.
Email: zakharov@geol.msu.ru

Geological Faculty

Russian Federation, bld. 1, Leninsky Gory, 119991 Moscow

A. L. Perchuk

Lomonosov Moscow State University; Academician Korzhinsky Institute for Experimental Mineralogy, Russian Academy of Sciences

Email: zakharov@geol.msu.ru

Geological Faculty

Russian Federation, bld. 1, Leninsky Gory, 119991 Moscow; bld. 4, Academician Hossipian Str., 142432 Chernogolovka, Moscow region

T. V. Gerya

Swiss Federal Institute of Technology

Email: zakharov@geol.msu.ru

Department of Earth Sciences

Switzerland, bld. 5, Sonneggstrasse, 8092 Zurich

M. D. Eremin

Lomonosov Moscow State University

Email: zakharov@geol.msu.ru

Geological Faculty

Russian Federation, bld. 1, Leninsky Gory, 119991 Moscow

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Supplementary files

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2. Fig. 1. Morphology and geometry of slabs in modern subduction zones (according to [44, 57, 100], with additions). Subduction zones: JAVA ‒ Javan; SUM ‒ Sumatran; IND ‒ Indian; KER ‒ Kermadec; TON ‒ Tonga; MAR ‒ Mariana; IZU ‒ Izu-Bonin; RYUK ‒ Ryukyu; HON ‒ Honshu; KUR ‒ Kuril; KAM ‒ Kamchatka; ALE ‒ Aleutian; ALYA ‒ Alaskan; KAS ‒ Cascade Mountains; CAM ‒ Central American; ANT ‒ Antilles; PER ‒ Peruvian; CHIL ‒ Chilean; SCO ‒ Scotia; CAB ‒ Calabrian; CRI ‒ Cretan. Denoted: boundaries of lithospheric plates (thin lines in blue); approximate position of cross sections and direction of subduction (arrows in blue); velocity of the subducting plate (cm/year) in the Indo-Atlantic hotspot system (Arabic numerals in blue near the arrows). Showed: schematic representation of slab morphology according to seismic tomographic models ‒ according to [44] (blue), according to [57] (purple); age of subducting plates, million years (Arabic numerals in red); base of the mantle transition zone at a depth of ~660 km (horizontal lines in black).

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3. Fig. 2. Scheme of metamorphic facies on the P-T diagram (according to [65], with modifications and additions). Geotherms for the plate surface under modern conditions (according to [69]) for subduction zones: cold (blue line), warm (red line); aqueous solidi of basalt (according to [82]) (green dashed line) and peridotite (according to [47]) (blue dashed line).

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4. Fig. 3. Main elements and initial state of the petrological-thermochemical 2D model. Model with additional mantle temperature ΔT = 150°C (Tp = 1450°C), convergence velocity v = 10 cm/yr, oceanic lithosphere age of 40 Ma and continental lithosphere thickness HL = 150 km. Inset: configuration of the pre-set subduction zone. Highlighted (dashed line contour): area shown in the inset. Isotherms are shown: with an interval of 200°C (thin lines in white), the boundary of the thermal lithosphere (thick line in white). 1 ‒ air; 2 ‒ water; 3-4 ‒ crust: 3 ‒ lower oceanic and continental, 4 ‒ upper oceanic; 5 ‒ sediments; 6-7 ‒ continental crust: 6 ‒ upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11-12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16-17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 ‒ melting from: a ‒ sediments, b ‒ metabasites

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5. Fig. 4. P‒T parameters of eclogitization of oceanic crust layers. (a)‒(b) – fields of eclogite formed from: (a) ‒ basalt; (b) – gabbro. Eclogitization parameters: I – Tb1 = Tg2 = 400°С and Tg1 = Tg2 = 600°С; II ‒ Tb1 = 450°С and Tb2 = 450°С, Tg1 = 600°С and Tg2 = 600°С; II ‒ Tb1 = 450°С and Tb2 = 500°С, Tg1 = 600°С and Tg2 = 650°С; IV ‒ Tb1 = 450°C and Tb2 = 550°C, Tg1 = 600°C and Tg2 = 700°C; V ‒ Tb1 = 450°C and Tb2 = 600°C, Tg1 = 600°C and Tg2 = 750°C; VI ‒ Tb1 = 450°C and Tb2 = 650°C, Tg1 = 600°C and Tg2 = 800°C; VII – Tb1 = 450°C and Tb2 = 650°C, Tg1 = 800°C and Tg2 = 1000°C. Denoted: boundaries of eclogitization parameters of the reference model (thin green lines), other models (dashed green lines); eclogitization temperature ranges for different models (arrows).

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6. Fig. 5. Parameters of numerical experiments. (A) – v = 5 cm/year; (B) ‒ v = 10 cm/year. Denoted: experiment numbers (Arabic numerals); eclogitization parameters (Roman numerals); eclogitization ranges (T, °C): basalt (blue), gabbro (red); additional mantle temperature (∆T, °C); convergence rate (v, cm/year); thickness of the continental lithosphere (HL, km).

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7. Fig. 6. 2D model of steep subduction development. Model No. 83: ∆T = 0 oC, v = 10 cm/year, HL = 80 km, Tb1 = 450°C and Tb2 = 650°C, Tg1 = 600°C and Tg2 = 800°C. A – substance: (a) – stage of gentle slab subsidence, (b) – increase in slab dip angle, (c) – steep slab dip in the upper mantle and flattening in the mantle transition zone (inset – density, kg/m3), (d) – slab bending in the transition zone; B – effective viscosity and velocity field (arrows): (d)–(h) correspond to (a)–(d), inset in (e) ‒ color scale of viscosity in logarithmic scale. 1 ‒ air; 2 ‒ water; 3‒4 ‒ crust: 3 ‒ lower oceanic and continental, 4 ‒ upper oceanic; 5 ‒ sediments; 6‒7 ‒ continental crust: 6 ‒ upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11‒12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16‒17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 – melted from: a ‒ sediments, b ‒ metabasites

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8. Fig. 7. 2D model of low-angle subduction development. Model #76: ∆T = 150°C, v = 10 cm/yr, HL = 80 km, Tb1 = 450°C and Tb2 = 650°C, Tg1 = 600°C and Tg2 = 800 °C. (a) – beginning of low-angle subduction; (b) – subcrustal rollback and steep dip of the leading part of the slab; (c) – detachment of the steeply dipping part of the slab and restoration of low-angle subduction; (d) – continuation of low-angle subduction with periodic detachments of a part of the slab. 1 – air; 2 – water; 3-4 ‒ crust: 3 ‒ lower oceanic and continental, 4 ‒ upper oceanic; 5 ‒ sediments; 6-7 ‒ continental crust: 6 ‒ upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11-12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16-17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 ‒ melting from: a ‒ sediments, b ‒ metabasites

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9. Fig. 8. 2D model of the transitional subduction regime. Model #73: ∆T = 150°C, v = 10 cm/yr, HL = 80 km, (Tb1 = 450°C and Tb2 = 500°C, Tg1 = 600°C and Tg2 = 650°C. (a) – gentle subsidence stage; (b) – subcrustal rollback and steep dip of the leading part of the slab; (c) – detachment of a part of the slab and continuation of steep subsidence; (d) – slab undercutting in the transition zone. 1 – air; 2 – water; 3-4 – crust: 3 – lower oceanic and continental, 4 – upper oceanic; 5 – sediments; 6-7 – continental crust: 6 – upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11‒12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16‒17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 – smelting from: a ‒ sediments, b ‒ metabasites

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10. Fig. 9. The effect of eclogitization parameters of basic oceanic crust on the subduction style. (a)‒(c) ‒ models #71, #73 and #76 (∆T = 150°C, v = 10 cm/yr, HL = 80 km) of eclogitization by eclogitization variants: (a) ‒ variant I (model #71, steep subduction, 13.3 Ma), (b) ‒ variant III (model #73, transitional subduction regime, 13.8 Ma), (c) ‒ variant VI (model #76, gentle subduction, 12.7 Ma). Inset: substance density (kg/m3). 1 ‒ air; 2 ‒ water; 3-4 ‒ crust: 3 ‒ lower oceanic and continental, 4 ‒ upper oceanic; 5 ‒ sediments; 6-7 ‒ continental crust: 6 ‒ upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11-12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16-17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 ‒ melting from: a ‒ sediments, b ‒ metabasites

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11. Fig. 10. The effect of additional mantle temperature ∆T on the subduction style. Models #61, #68, #75 and #82: v = 10 cm/yr, HL = 80 km, eclogitization parameters according to variant V (Tb1 = 450°C and Tb2 = 600°C, Tg1 = 600 °C and Tg2 = 750°C). (a) – ΔT = 0°C (model #82, steep subduction, 13.6 Ma); (b) – ΔT = 150°C (model #75, transitional regime, 13.8 Ma); (c) – ΔT = 200°C (model #68, low-angle subduction, 13.4 Ma); (d) – ΔT = 250°C (model #61, low-angle subduction, intraplate deformation, 13.1 Ma). The models are arranged in order of increasing ΔT. 1 ‒ air; 2 ‒ water; 3-4 ‒ crust: 3 ‒ lower oceanic and continental, 4 ‒ upper oceanic; 5 ‒ sediments; 6-7 ‒ continental crust: 6 ‒ upper, 7 ‒ middle; 8 ‒ depleted mantle (>20%); 9 ‒ mantle; 10 ‒ weakened zone; 11‒12 ‒ mantle: 11 ‒ serpentinized, 12 ‒ hydrated; 13 ‒ granitoids and felsic volcanics; 14 ‒ basalts from dry mantle; 15 ‒ basalts: a ‒ partially melted, b ‒ melted from hydrated mantle; 16‒17 ‒ partially melted mantle: 16 ‒ dry, 17 ‒ hydrated; 18 ‒ restite from melting of hydrated mantle; 19 ‒ partially melted: a ‒ sediments, b ‒ metabasites; 20 – melting from: a ‒ sediments, b ‒ metabasites

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12. Fig. 11. Generalization of the results of numerical 2D modeling with different initial parameters. (A) – v = 5 cm/year; (B) ‒ v = 10 cm/year. Designated: experiment numbers (Arabic numerals); eclogitization parameters (Roman numerals); eclogitization ranges (T, °C): basalt (blue), gabbro (red); additional mantle temperature (∆T, °C); convergence rate (v, cm/year); thickness of the continental lithosphere (HL, km).

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13. Fig. 12. Scheme of subduction styles depending on the control parameters of all the models considered.

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