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Volcanic and igneous plumbing systems

Volcanic and igneous plumbing systems is a earth science topic covered in the lgStudy science library. This page brings together a partial reference excerpt, illustrations, worked examples, real-world applications and a short study plan, so you can understand Volcanic and igneous plumbing systems rather than just read about it. In short: Volcanic and igneous plumbing systems (VIPS) consist of interconnected magma channels and chambers through which magma flows and is stored within Earth's crust. Volcanic plumbing systems can be found in all active tectonic settings, such as mid-oceanic ridges, subduction zones, and mantle plumes, when magmas generated in continental lithosphere, oceanic lithosphere, and in the sub-lithospheric mantle are transported.

Volcanic and igneous plumbing systems — main illustration
Volcanic and igneous plumbing systems — illustration

Key takeaways

  • Volcanic and igneous plumbing systems belongs to earth science; place it in that map before memorising details.
  • Learn the definition first, then one example that makes the definition concrete.
  • Connect Volcanic and igneous plumbing systems to a quantity you can measure, compute or draw — that is where exam questions come from.
  • Reproduce the core statement of Volcanic and igneous plumbing systems from memory before moving on to harder problems.

Reference excerpt

Volcanic and igneous plumbing systems (VIPS) consist of interconnected magma channels and chambers through which magma flows and is stored within Earth's crust. Volcanic plumbing systems can be found in all active tectonic settings, such as mid-oceanic ridges, subduction zones, and mantle plumes, when magmas generated in continental lithosphere, oceanic lithosphere, and in the sub-lithospheric mantle are transported. Magma is first generated by partial melting, followed by segregation and extraction from the source rock to separate the melt from the solid. As magma propagates upwards, a self-organised network of magma channels develops, transporting the melt from lower crust to upper regions. Channelled ascent mechanisms include the formation of dykes and ductile fractures that transport the melt in conduits. For bulk transportation, diapirs carry a large volume of melt and ascent through the crust. When magma stops ascending, or when magma supply stops, magma emplacement occurs. Different mechanisms of emplacement result in different structures, including plutons, sills, laccoliths and lopoliths.

Magma production

Partial melting Partial melting is the first step for generating magma and magma is the basis of VIPS. After magma is generated, it will travel across the crust and lead to the formation of magma conduits and chambers. In continental crust, partial melting occurs when a portion of the solid rock melts into felsic magma. Rocks in the lower crust and the upper mantle are subject to partial melting. The rate of partial melting and the resultant silicate melt composition depend on temperature, pressure, flux addition (water, volatiles) and the source rock composition. In oceanic crust, decompression melting of mantle materials forms basaltic magma. When the mantle materials rise, the pressure greatly decreases which significantly lowers the melting point of the rock.

Melt segregation and extraction

After magma is generated, magma will migrate out of its source region by the process of magma segregation and extraction. These processes define the resulting composition of the magma. Depending on the efficiency of the segregation and extraction, there will be different structures of the volcanic and igneous plumbing systems.

Segregation Melt segregation is the process of melt separating from its source rock. After the silica-rich melt is generated by partial melting, melt segregation is achieved by the gravitational compaction of the source rock. It causes the squeezing of the melt through the pores and the melts are produced at grain boundaries. When the melt droplets continue to build up and the proportion of melt continues to increase, they tend to gather together as melt pools. The interconnectivity of the melt determines whether and when melt may be extracted. When the melt percentage in the source rock approaches the first percolation threshold at 7%, the melt starts to migrate. At this point, 80% of the grain boundaries are melted and the rock becomes very weak. As melting advances and the melt continues to accumulate, it reaches the second percolation threshold at a melt percentage of 26% to 30%. The matrix of the source rock will start to break down and the melt will start to be extracted.

Extraction After the melt segregates from the solid, melt extraction takes place. The rate of magma extraction depends on the spatial distribution and interconnectivity of the magma channel network developed out of its source rock. There are two end members of melt extraction: melt can be extracted in pulses if the development of magma channels are rapid and the network is highly interconnected, or melt can be constantly drained from the source if the magma channels are developed in a continuous and steady manner. Also, magma extraction controls the chemical composition of the melt, the amount of magma transported by dykes, and consequently, the volume flux of magma into plutons. These will eventually control the overall structure of the VIPS such as the formation of dykes and plutons. For instance, if the magma channels are not well connected, the source may not be drained successfully, and dykes may freeze before propagating far enough to feed plutons. If the source rock could not initiate dyke ascent with sufficient melt, the source rock may remain undrained, favouring diapiric ascent of the source rock.

Magma ascent and transportation When there is sufficient melt accumulation, the magma in the source will migrate from the source to the shallower level of the crust through magma conduits to feed and form different magma reservoirs and structures in VIPS. The buoyancy of magma is the main driving force of all types of transportation mechanism.

… excerpt ends here. Continue reading the full article.

Illustrations

Volcanic and igneous plumbing systems: Schematic sketch of the volcanic and igneous plumbing systems (after Burchardt, 2018).[1][2]
Schematic sketch of the volcanic and igneous plumbing systems (after Burchardt, 2018).[1][2]
Volcanic and igneous plumbing systems: Microscopic view of melt segregation and extraction.[6][7][8] When the source rock experiences compaction, minerals start to melt at grain boundaries. Melt droplets then build up and connect into melt pools until they are being extracted.
Microscopic view of melt segregation and extraction.[6][7][8] When the source rock experiences compaction, minerals start to melt at grain boundaries. Melt droplets then build up and connect into melt pools until they are being extracted.
Volcanic and igneous plumbing systems: End members of magma segregation, ascent, and displacement: Diapirism and Channeled ascent (after Cruden, 2018).[4] Diapirs transport melt in a large batch of magma and emplace as plutons. Transport channels transports melt in a fracture network and emplace as dykes and sills.[4]
End members of magma segregation, ascent, and displacement: Diapirism and Channeled ascent (after Cruden, 2018).[4] Diapirs transport melt in a large batch of magma and emplace as plutons. Transport channels transports melt in a fracture network and emplace as dykes and sills.[4]
Volcanic and igneous plumbing systems: Pegmatite dyke intruding quartzite in Marquenas Formation, New Mexico, United States
Pegmatite dyke intruding quartzite in Marquenas Formation, New Mexico, United States
Volcanic and igneous plumbing systems: Shape of different magma emplacement structures: (a)sill, (b) pluton, (c) laccolith and (d) lopolith.[4] Sills are tabular sheet intrusions. Plutons are large, thick tabular bodies. Laccoliths are dome-shaped structures with elevate roofs and flat floors. Lopoliths are lenticular structures with flat roofs and depressed floors.[4]
Shape of different magma emplacement structures: (a)sill, (b) pluton, (c) laccolith and (d) lopolith.[4] Sills are tabular sheet intrusions. Plutons are large, thick tabular bodies. Laccoliths are dome-shaped structures with elevate roofs and flat floors. Lopoliths are lenticular structures with flat roofs and depressed floors.[4]

Worked examples

Example 1 — a first encounter with Volcanic and igneous plumbing systems

Start with the simplest possible case. Write down what Volcanic and igneous plumbing systems claims or describes in one sentence, then invent the smallest concrete situation in which that sentence is true. In earth science, the smallest case is usually a single object, a single equation or a single measurement. Check that every symbol or term in your sentence has a meaning in that case.

Example 2 — changing one variable

Take the situation from Example 1 and change exactly one quantity: double it, halve it, or set it to zero. Predict what should happen to Volcanic and igneous plumbing systems before you calculate. Comparing your prediction with the result is the fastest way to find out whether you understand the idea or only the words.

Example 3 — an exam-style question

Typical questions about Volcanic and igneous plumbing systems ask you to (a) state it precisely, (b) apply it to given data, and (c) explain a limitation. Practise writing all three answers in under five minutes; the third part is what separates a full-mark answer from an average one.

Applications of Volcanic and igneous plumbing systems

In research
Volcanic and igneous plumbing systems appears in earth science research whenever the underlying quantities have to be modelled precisely. Papers usually cite it as a starting assumption and then explore where it breaks down.
In technology and industry
Engineering practice reuses Volcanic and igneous plumbing systems in design rules, simulations and safety margins. Knowing the idea lets you read a specification sheet and understand why the numbers look the way they do.
In the classroom
Volcanic and igneous plumbing systems is common in secondary-school and first-year university syllabi. It links to neighbouring topics Lithosphere, Volcanism, so understanding it makes those chapters shorter.
In everyday life
Look for Volcanic and igneous plumbing systems outside the textbook — in sport, cooking, traffic, electronics or the sky above you. An example you found yourself is remembered far longer than one you were given.
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How to study Volcanic and igneous plumbing systems in 20 minutes

  1. Read the reference excerpt below once, without taking notes.
  2. Close the page and write down what Volcanic and igneous plumbing systems means in your own words.
  3. Compare your version with the excerpt and mark what you missed.
  4. Work through the three examples above with pen and paper.
  5. Explain Volcanic and igneous plumbing systems out loud to somebody else — or to Teacher Smith in the lgStudy chat.

Frequently asked questions

What is Volcanic and igneous plumbing systems in simple terms?

Volcanic and igneous plumbing systems (VIPS) consist of interconnected magma channels and chambers through which magma flows and is stored within Earth's crust. Volcanic plumbing systems can be found in all active tectonic settings, such as mid-oceanic ridges, subduction zones, and mantle plumes, w…

Why does Volcanic and igneous plumbing systems matter?

Because it connects several earth science ideas at once: it gives you a definition you can apply, a quantity you can calculate, and a way to check whether a result is plausible.

How should I study Volcanic and igneous plumbing systems?

Read the excerpt, restate it from memory, then work through the examples and applications listed on this page. The five-step study plan above takes about twenty minutes.

What does this page cover?

It gives you a compact reference excerpt plus original lgStudy explanations, examples, applications and study material on Volcanic and igneous plumbing systems.

Tags

  • Lithosphere
  • Volcanism

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