Structure of the Earth
When studying plate tectonics, the best starting point is to examine the Earth’s structure. The Earth is divided into a series of layers: the inner core, outer core, mantle and crust. Each of these layers has its own chemical and mechanical properties.
Cross-section of the Earth illustrating oceanic and continental crust.
The outermost layer of the Earth is the crust. The crust is the thinnest layer. There are two types of crust: oceanic and continental.
Continental crust, varying in thickness from 20 to 200 kilometres, is not as dense as its oceanic counterpart. Primarily composed of granite, this crust is indestructible and significantly older than oceanic crust, reaching up to 3.8 billion years.
In contrast, the oceanic crust, with a thickness ranging from 5 to 10 kilometres, consists predominantly of dense basalt. When oceanic crust converges with continental crust at a destructive plate boundary, it descends into the mantle. This is known as subduction. Notably, the oceanic crust is much younger than the continental crust, being less than 200 million years old.
The Structure of the Earth
The crust and the upper mantle form the lithosphere, which is solid and brittle, and is approximately 100 km thick.
The lithosphere is divided into large sections, known as tectonic plates. Tectonic plates consist of sections of the lithosphere. The oceanic lithosphere is topped by oceanic crust, and the continental lithosphere is topped by continental crust.
A common misconception is that the mantle is made of liquid magma. In fact, it is made of solid rock.
The section of the Earth’s mantle beneath the lithosphere, extending from a depth of approximately 100 kilometres to 400 kilometres, is known as the asthenosphere. The lithosphere and asthenosphere have a similar chemical composition. However, they have different mechanical properties. The lithosphere is brittle, whereas the asthenosphere is solid but ductile (plastic-like, it will flow over a very long timescale). In the asthenosphere, as depth increases, so does the temperature, reaching at least 1300°C. This temperature is sufficient to melt peridotite (the material that makes up the mantle) under surface conditions. However, the high pressure at such depths prevents the peridotite from melting. As a result, it stays solid yet is ductile, allowing it to flow.
The lower mantle remains ductile but denser due to the increased pressure.
The outer core is made up of liquid iron and nickel. The inner core, a solid mass of iron and nickel, forms the Earth’s centre. The core’s temperature is approximately 5500°C.
